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O rder N u m b e r 9 1 2 9 4 3 7

T he glacial geom orphology o f th e P ort H uron C om plex in
northw estern southern M ichigan
Blewett, William Llewellyn, Ph.D.
Michigan State University, 1991

UMI

300 N. Zeeb Rd.
Ann Arbor, MI 48106

THE GLACI AL G E O M O R P H O L O G Y OF THE PORT H U R O N C O MP LE X
IN N O R T H W E S T E R N S O U T H E R N MIC HI GA N
By
W i l l i a m L l e w e l l y n Blewett

A DISSERTATION

S u b m i t t e d to
M i c h i g a n State U n i v e r s i t y
in parti al f ul f il lm ent of the re qu ire men ts
for the d e g r e e of

D O C T O R OF P H I L O S O P H Y
Department

of G e o g r a p h y

1990

A B S T R A CT
THE G LA CI A L G E O M O R P H O L O G Y OF THE PORT H U R O N C O M P L E X
IN N O R T H W E S T E R N S O UT HE RN M I CH IG AN
By
W i l l i a m L l e w e l l y n Blewett

This

study

investigates

the morphologic,

s e d i m e n t o l o g i c , and ch ro n o l o g i c
T a y l o r ’s (1915)
Kalkaska,

and

Inner and O u t e r Port H ur on M o r a i n e s

Antrim,

Counties.

l a n d f o r m units are

1) the O u t e r Port H u r o n Complex,

Port H u r o n C o m p l e x
the Post

in

ea s t e r n C h a r l e v o i x and w e s t e r n Otse go

Four p r i n c i p a l

include

aspect s of L ev er et t and

(incl ud in g

Inner Port H u r o n

re co g n i z e d
2) the

the M a n c e l o n a Plain),

zone,

and 4)

Inner
3)

flu te d u p l a n d s

and

throu gh valleys.
Surficial

sediments

of the

Inner and O u t e r Port H u r o n

C o m pl ex es are alm os t e x c l u s i v e l y
and gravel,

and 2)

is almost w ho l l y
Post

1) g l ac io f l u v i a l

glaciolacustrine

r es tr i c t e d

to the

Inner Port H u r o n zone.

The

sand

silt and clay.
fluted u p l a n d s

Inner and O u t e r

Till
and

the

features

each co nt a i n an u p p e r m o s t we dge of sand and gr a v e l up to
80 m thick,

d e p o s i t e d on a m o d e r a t e

inclined to the northwest.
contac t and p r o g l a c i a l

relief till

surface

Cresta l areas ex hi bi t

s t r a t i f i e d drift and

ice-

surf ic ia l

bo ul de rs

as so c i a t e d w i t h d e p o s i t i o n along m a r g i n a l l y

stagnant

ice.

Thus,

textured glacial

pro xi ma l

till"

sediments

are not

as map pe d by others

"coarse

(Fa r r a n d and

Bell,

1982),

especially

but,

of

r e l a t e d to the m a i n surface of the

Mancelona Plain
poorly

(Elmi ra surface)
sor te d pr ox ima l

lo n g i t ud in a l bars

to distal,

show a t r a n s i t i o n

Paleocurrent

indicators

fine textured,

well-sorted

sandy bedforms.

show that m e l t w a t e r

flowed p e r p e n d i c u l a r l y away from the
90 d egr ee s

to the right

from

de po si ts d o m i n a t e d by

br a i d e d str eam d e p o s i t s d i s p l a y i n g

turned

facies

i m p or tan t heads of outwash.

Sedi men ts

coarse,

instead are pro xim al

to

streams

first

ice m a r g i n and then

flow pa ra lle l

to the

s a n d u r ’s axis.
The M a n c e l o n a P l a i n and Post Port Hu ro n zone c o nt ai n
10 and

16 sep ara te

Collectively,
qu a s i - st ab l e

these

o u t w a s h surfaces,
su rfaces

ice-marginal

ou t w a s h deposition,
p er io ds of rapid

rec or d long

c o n d it io ns

pu nc tu a t e d

intervals

favoring

of

thick

by brief tr an si ti on al

i n ci s i o n due to

L an d f o r m and s e d i m e n t

respectively.

ice-m arg ina l

relationships

retreat.

show that this

retreat was c h a r a c t e r i z e d by an ice ma rg i n that pivot ed
cl o ck wi se
The

to the n o r t h w e s t dur in g

final d eg la ci at io n.

Inner and O u t e r Port H u r o n Co mp le xe s both

d is p l a y a d i s t i n c t
Lo c at io ns

of the

s al ie nt and re entrant pattern.

fo rm e r are c l o s e l y relat ed to the

ma g n i t ud e of lower areas on the d e e p l y bu ri e d b e d r o c k
surface.

Both c o m p l e x e s

pro f i le s

in cr o s s- se c ti on ,

conta ct

slopes

1) d i s p l a y al luvial
2)

exhib it pr o m i ne nt

t r e n d i n g tens of kil om et er s

and 3) have h u m m o c k y pr ox i m a l

fan-like
ice-

in some areas,

regions d i s p l a y i n g hanging

valleys,

pe rc h e d

fans,

and d i s i n t e g r a t i o n ridges.

C om b i n e d wi t h s e d i m e n t a r y evidence,
as s e m b l a g e s

indicate

that

su cc e s si ve m a r g i n a l l y

these l a n d f o r m

the t e rr ai n formed along

st ag na nt glacial te rm in ii

by at least nine m o r p h o s e q u e n c e s

defin ed

(Koteff and Pessl,

1981 ) .
Finally,
with

w o o d and ot her organ ic ma te ria l a s s o ci at ed

la cus tr ine

silts

lo cat ed 50 m below the M a n c e l o n a

Pl ain yi eld an age es ti m a t e
Elsewhere,
pr ov i d e s

carbonaceous material

a m i n i m u m date of

Port H u r o n Complexes,
determinations
that

the

be t w e e n
agre es

of >41,000 y r s . B.P.

and,

from l ac us tr in e deposits

12,960

+ 350 yrs.

Inner an d O u t e r Port H u r o n Co m p l e x e s
14,000

yrs.

B.P.

s t r o n g l y w i t h age e s t i m a t e s

the Port H u r o n M o r a i n e
a l . , 1957;

Calkin,

in Ohio

1970),

1915),

m i n i m u m date

and 3),

formed
1)

for c o r r e l a t i v e s of

and O n ta ri o

(B a r e n d s e n et

2) helps ve r i f y c o r r e l a t i o n of

for the

(Leverett and

first time,

for the Port H u r o n Comp le xe s

s o u t h e r n Michigan.

indicates

This e s t i ma te

the Port H u r o n C o m p l e x w i t h i n M i c h i g a n
Taylor,

for the

c o m b i n e d with age

from the Lake B o r d e r Moraine,

13,000 and

B.P.

pr o v i d e s a
in n o r t h w e s t e r n

for G r e t c h e n
and
for ray fam il y

v

ACKNOWLEDGMENTS

I w i s h to s i n c e r e l y t h a n k my c o m m i t t e e m e m b e r s Dr.
Harman,

Dr.

patience,

the

and Dr.

J. W i n k l e r

and c o n s t r u c t i v e

study.

insights,

pe rs o n a l
wer e

Schaetzl,

guidance,

throughout
helpful

R.

Dr.

access

David

c o p y of M e l h o r n ’s di ss er tat ion ,
Dr.

D.

laboratory

space

White,

all

and a

of whi ch

M o k m a and the

of C r o p and Soil S c i e n c e s

0.

criticism

Lusch also p r o v i d e d

Department

Dr.

for their

to ae r ia l ph ot ogr aph s,

g r e a t l y appre ci at ed .

J.

g e n e r o u s l y pr o v i d e d

and acc es s to the x - r a y d i f f r a c t o m e t e r .

A n d e r sl an d ,

Dr.

G.

M a s e , Dr.

B.

Pigozzi,

and Mat t J o h n s t o n e p r o v i d e d t e c h n i c a l

T h a n k s also

to Mike Blum,

who p r o v i d e d

Ellen

assistance.
the

link with

the U n i v e r s i t y of Texas at A u s t i n ’s r a d i o c a r b o n
l aboratory,

spent

a c ra sh co ur s e
J.

sever al

da y s

in the

in b e d f o r m l i t h o f a c i e s

field,

id en ti fic ati on;

K nox of the U n i v e r s i t y of Wi sconsin,

in sights and e n c o u r a g e m e n t ;
Il li n o i s U n i v e r s i t y
and g e n e r o u s

for m or al

insights;

Dr.

c o n s t r u c t i v e critcism;
d is cus sio ns;

support,

for his

field disc uss ion ,

b e d r o c k maps;

of the Au Sable

Gr ah a m e

Madiso n,

Institute

L a r s o n for his

Bill Mo na gha n,

Cal
for

int er es t

for e a r l y

W a r r e n S t u d l e y of the Soil C o n s e r v a t i o n

vi

Dr.

R i c h a r d R i e c k of W e s t e r n

s h a r i n g of u n p u b l i s h e d

Dewit t and T a r a D e V r i e s
their

Dr.

an d pr o v i d e d

and

Servic e

for the a r c h e o l o g y

p h y s i c i s t Ad a m B u r n e t t
com pl aining;
trip;

for l i st en ing

Ma rk Kumler,

Ch ar li e Ra de r

field trip;

for steali ng my field notebooks;

field of fi c e

(Rattlesnake Death)

them.

and the

for p r o v i d i n g the Lake

The

his

staff of the D N R ’s

Cabin for use during

field seasons.

wi th ou t

and for not

indebted to D e n n y Vitton,

p r e d e c e s s o r Don Hennig,

1989

en couragement,

and

in the meantime.

I am e s p e c i a l l y

Kalkaska

to my con stant

for the B o a r d m a n R iv er canoe

G r e t c h e n Kuhn for support,
d i v o rc in g me

f ru st ra te d

the

Skegemog
1988 and

study w ou ld have been

The D N R ’s Ge ol og ic al

impossible

Sur ve y Di v i s i o n also

pr o v i d e d copies of w a t e r and p e t r o l e u m well

logs

free of

charge.
Finally,

thanks to the

n o r t h e r n M i c h i g a n wh o

friendly,

freely g r a n t e d access to their

p r o p e r t y and sh o w e d genui ne
special

note are Mr.

W e s t p h a l ; and Mr.
K i t c h e n Farms,
Gravel,

interest

Sha ro n Crego,

in the study.

Mr.

Cash Polls of Elmira;

Alba;

and Mr.

ge ne r o u s peo pl e of

and Mr.

Ro y Wilk es

and Mrs.

Of

Carl

Mr. Bob K i tc he n of

R i c h a r d K le rr of C and K

of Wil ke s Excavating,

both

Mancelona.
Mos t of all
H a r o l d Winters,
at all

I am d e ep ly

for his guidance,

stages of the study.

advisor,

ind ebted to my advisor,
patience,

As a teacher,

and role model he is wi th ou t peer.

vii

and

Dr.

interest

researcher,

T AB LE O F C O N T E N T S

Page
CHAPTER

1

I N T R O D U C T IO N

1

Background
Pr o b l e m stat em en t
B a c k g r o u n d and me t h o d s
D e f in i t i o n s and co nc e p t s
T e c hn i q u e s
Study area
Li te rat ur e revi ew
R ev i e w of san dar
Justification

CH A P T E R

1
4
5
5
9
11
14
20
21

2

P A L E O Z O IC B ED R O C K AND Q U A T E R N A R Y
SE D I M E N TS A S S O C I A T E D WITH THE
INNER AND O U T ER PORT H U R O N CO MPLEXES:
R E V I E W A N D NEW FI ND I N G S
Bedrock geology
B e d r o c k surfa ce
Bedrock topography
Bedrock valleys
R e l a t i o n s h ip of the b e d r o c k surfa ce to t o p o g r a p h y
R e l a t i o n s h i p b e t w e e n t h r o u g h v a l l e y s and b e d r o c k
va lle ys
C o nc lu si on s
Sedim ent s a s s o c i a t e d w i t h the Inner and O u t e r Port
H u r o n Co m p l e xe s
Drift th ic kne ss
Re l a t i o n of drift, b e d r o c k form, and m o d e r n
to p og r ap hy
S ub su rf ace s t r a t i g r a p h y
Sub su r f a ce s ed im ent s a s s o c i a t e d wi t h the Inner
Port H u r o n C o m p l e x
Sub su rfa ce sedi men ts a s s o c i a t e d wi t h the Ou te r
Port H u r o n C o m p l e x
Rugg Pond site
Surf ici al se di me nt s
Surficial se di men ts of the Inner Port H u r o n
Co mpl ex
C o m p a r i s o n of sed ime nt c h a r a c t e r i s t i c s among
gravel pits
vi i i

24
24
26
26
28
29
34
34
36
36
37
40
41
46
47
50
51
53

S t o ne p i l e s
Bedfo rms
Paleocurrents
Paleodischarge
Till a s s o c i a t e d wi t h the Inner Port H u r o n
C o m pl ex
Se diments a s s o c i a t e d w i t h the Post Inner Port
H u r o n zone
Sur ficial se d i m e n ts a s s o c i a t e d wit h the O u t e r
Port H ur on C o m p l e x
Evi dence for facies chang es in the O u t e r Port
Huron Complex
Boulder d i s t r i b u t i o n
Soils
Textu re and li th ol og ic co mp ar i s o n of tills from
the study a r e a
Su mm ar y

61
61
73
73
79
79
84
86
86
88
90
95

CHAPTER 3
L A N DF OR MS A S S O C I A T E D W ITH THE INNER
A N D O U T E R PORT H U R O N C O M P L E X E S

97

Bedrock/landform relationships
97
La n d f o rm s a s s o c i a t e d w i t h the Inner Port H u ro n
Co m pl e x
99
Pr oximal tracts
100
Fluvial and g l a c i o f l u v i a l su rfaces of the
Mancelona Plain
103
C r o f t o n surfa ce
105
Surface 1
105
Elm ir a surfa ce
108
Te rr ac es 3-8
112
Ho f f m a n Lake Chann el
113
La n d f o r m s of the Post Inner Port H u ro n zone
114
Surfac e A
118
Surfac es B, C, and D
118
Surfac es of the C e d a r - G r e e n river v a ll ey
118
Surfac es of the J o r d a n R i v e r - W a r n e r Cr ee k v a l l e y 119
Landf or ms a s s o c i a t e d w i t h the O u t e r Port H u r o n
Complex
120
N o r t h e rn pr ox im a l regio ns
121
Fleming D i s i n t e g r a t i o n Ri d g e s
121
Lake 27 D i s i n t e g r a t i o n Rid ge s
121
El m i r a S o u th A p r o n
122
Abandoned Farm Hummocks
122
A l b a S a li en t
122
A l b a South A p r o n
124
Mancelona Reentrant
124
N o r t h e rn di st a l tracts
126
Mul t ip l e m ar g i n s of the s o u t h e r n Outer Port
H u r o n C o mp lex
127
Con cl us io n s
129
ix

CH A P T E R 4
PR OP O S ED D E G L A C I A T I O N AND L A N D F O R M
D E V E L O P M E N T IN THE STUDY
AREA
Phase 1
Phase 2
Phase 3
Phase 4
Phase 5
Phase 6
Region al c o r r e l a t i o n
Correlation within Michigan
Age d e t e r m i n a t i o n s for the Port Hu ro n C o m p l e x
northern Michigan
C o n c l u s i o ns

CH A P T E R

133
135
139
142
148
150
152
153
155
in
156
160

5

CO N C L U S I O N S AND

I M P L I C A T IO NS

S e d i m e n t o l o g i c findin gs
M o r p h o l o g ic fin dings
C h r o n o l o g ic findings
S u g g e sti on s for furth er r e s e a r ch

162
162
164
168
169

APPENDIX A
FIELD AN D L A B O R A T O R Y T E C H N I Q U E S
Field t e c h n i q u e s
Gravpl pits and ot he r e x p o s u r e s
S u r fi ci al se di m en t study
Laboratory techniques
Sand and gra ve l
Till

172
172
172
173
174
174
175

AP P E N D I X B
CLAY M I N E R A L O G Y

176

LIST OF R E F E R E N C E S

181

x

LIST OF TA B LE S

Ti tl e

Table
1

2

L i t h o f a c i e s and s e d i m e n t a r y s t r u c t u r e s
of fl u v ia l d e p o s i t s (from Miall, 1978).

64

Bedform lithofacies
the E l m i r a surface.

67

3

Paleodischarge

4

Soils

5

Co l o r and
tills.

6

7

Page

of gravel pits on

estimates.

78

of the s t u d y area.

89

clay m i n e r a l o g y of p r i n c i p a l
91

C h a r a c t e r i s t i c s of pr ox im al s u b d i v i s i o n s
of the O u t e r Port H u r o n Complex.

125

C h a r a c t e r i s t i c s of mu l t i p l e
m a r g i n a l positions.

130

xi

ice-

LIST OF FI GUR ES

Figur e
1

2

3

4

5

6

7

8

9

10

11

Page

T i tl e
The Port H u r o n M o r a i n e in sou th er n
M i c h i g a n (after L e v e r e t t and Taylor,
1915 ) .

2

L a n d f o r m s and s e d i m e n t s a s s o c i a t e d
w i t h a st ag n a nt ice m a r g i n (from
B l e w e t t , 1984 ) .

7

M a j o r l a n d f o r m g r o u p s as mapped by
M a r t i n (1955).

12

Major landform groups
this study.

13

re co g n i z e d

in

B e d r o c k ge ol o g y (from Milstein, 1987),
s ho wi n g the r e l a t i o n s h i p with the
I nne r a n d O u t e r Port H u r o n Complexes.

25

B e d r o c k t o p o g r a p h y ( © 1981, 1985,
R. L. R i ec k; used w i t h pe rm ission).

27

P r o f i l e A-A, ’ s h o w n on Figure 5, sh o w i n g
the r e l a t i o n s h i p of the b e d r o c k s u r f a c e
to topography.

30

P r o f i l e B - B , ’ s h o w n on Figure 5, sh o w i n g
the r e l a t i o n s h i p of the be d r o ck su rf a c e
to top ogr aph y.

32

P r o p o s e d ge nes is of c oi nc id en t v a l l e y s
(from Ble wett, 1984).

35

D ri ft t h i c k n e s s in the
Port H u r o n Compl ex es .

38

Inner an d O u t e r

T h i c k n e s s of the u p p e r m o s t
gr a v e l unit.

sand and

12

Altitude

clay surface.

13

R e l a t i o n b e t w e e n m o d e r n t o p o g r a p h y and
the u n d e r l y i n g c l a y surface.
Profile
l o c a t i o n shown in Fi g ur e 5.

44

Rugg P o n d S t ra ti gra phy .

49

14

of the u n d e r l y i n g

xii

42
43

15

M a p of the s u r f i c i a l se d i m e n t s of the
Inner and O u t e r Po r t H u r o n C om ple xe s,
n o r t h w e s t e r n s o u t h e r n Michigan.
(in

16

O v e r a l l d i s t r i b u t i o n of co a r s e an d
sediments.

17

18

19

20

21

22

23

24

25

fine
52

Ro un d n e s s , flatness, and s p h e r i c i t y of
c o a r s e c l a s t s fr o m gr a ve l pits on the
E l m i r a surface.

54

M e a n B - a x i s d i a m e t e r of coarse cl as t s
fr om g ra v e l pits on the El mi r a surface.

55

M e a n s p h e r i c i t y of coa rs e cla st s fro m
g r a v e l pits on the E l m i r a surface.

57

B - a x i s v a r i a n c e of coa rs e cla st s from
g ra v e l pits on the E l m i r a surface.

58

D i s t r i b u t i o n of "ve ry angular" c o ar se
c l a s t s fro m gra ve l pits on the E l m i r a
surface.

59

D i s t r i b u t i o n of c o a r s e and fine
s e d i m e n t s from grav el pits on the
E l m i r a surface.

60

M e a n B - ax is d i a m e t e r of
the E l m i r a surface.

stone p i l e s

on
62

Bedform lithofacies associated with
the E l m i r a o u t w a s h surface.

65

S e d i m e n t s at the C and K gravel
(proximal), Mancelo na.

68

pit

S a n d y b e d f o r m s at the Lower W i l k e s
g r a v e l p i t (medial), Mancelona.

69

L i t h o f a c i e s Sh at the D NR sand pit
(distal), Kalkaska.

71

28

P a l e o c u r r e n t s on the E l m i r a surface.

74

29

S t r a t i g r a p h y at the A n t r i m C o u n t y
Ro a d C o m m i s s i o n gra ve l pit.

81

26

27

30

Soil te x t u r e s of p r i n c i p a l
the s t u d y area.

tills

in
92

o

31

F r e q u e n c y d i a g r a m of 7/10 A rati os
for t i l l s in the st ud y area.

xiii

94

32

33

34

Lan df or ms of the I nn er and O ut er
Port H u r o n Complexes.

(in pocket

R e l a t i o n s h i p among salients, reentrants,
t h ro ug h valleys, re si du al terraces,
and b e d r o c k valleys.
Pr i n c i p al
Plain.

sur faces

98

of the M a n c e l o n a
104

35

Pr of i l e s

36

V i e w s o u t h e a s t w a r d acro ss the E l m i r a
Pl ai n near Alba; the pr oximal slope of
the O u t e r Port H u r o n Co mpl ex is in the
distance.

110

View from the D e a d m a n ’s Hill ov e r l o o k
of the u n d e r f it Jor da n River w i t h large
paleomeanders.

116

P r i n c i p a l g l a c i o f l u v i a l / f l u v i a l surfaces
of the C e d a r - G r e e n and J o r d a n - W a r n e r
valleys.

117

V i e w of pr ox i m a l h u m m o c k y to po g r a p h y
at the A b a n d o n e d F a r m site in the O ut er
Port H u r o n Complex.

123

P ro f i l e across
Complex.

128

37

38

39

40

41

42

of s e l e ct ed

sandar.

109

the O u t e r Port H u r o n

Mod el s of d e p o s i t i o n
Plain.

for the M a n c e l o n a
134

Phase 1. F o r m a t i o n of the O u t e r Port
H u r o n Complex.

136

43

F o r m a t i o n of the C r o f t c n surface,

140

44

Phase 2.

Formation

of Surfac e

1.

141

45

Phase 3.

Formation

of Surfac e

2.

143

46

F o r m a t i o n of su rf a c e s

47

Phase 4.

48

F o r m a t i o n of the J o r d a n - W a r n e r and
C e d a r - G r e e n river systems.

Formation

xiv

3 and 4.

of surfa ce

145
A.

147

149

49

50

R e a d v a n c e after f o r m a t i o n
of the Post Inner Port H ur on zone.

151

X-ray diffractograms.

178

xv

C h ap t e r 1

I N TR OD UC TI ON

B a ck gr ou nd
The Port H u r o n M o r a i n i c
most c on sp i c u o u s
Michigan

C o m p l e x marks one of the

t o p o g r a p h i c co m p l ex es

(Le ve r e t t

and Taylor,

1915,

in sou the rn

p.

293)

and is

i n t e r p re t e d as the o ute r limit of a s i g n i f ic an t
readvance
Eschman,
Taylor

c.

13,000

1974;

(1897,

mo ra in e was

yrs.

B.P.

Fullerton ,
p.

41-43)

(Hough,

1980).

in s o u t h e a s t e r n Michigan,

L ev er et t

and T a y l or

e xt en de d

no rt h and w e s t w a r d near ly

(1915)

and,

306)

broad,

relatively

in g re at er detail

550 km.
(Fig.

by

Mappi ng

1).

Lev erett

in the n o r t h w e s t e r n part of the

(L everett and Taylor,

and re co gn i z e d an

the

at the same time,

was ba sed p r i m a r i l y on m o r p h o l o g y

So u t h e r n P e n i n s u l a

Fa r r a nd and

First r e c o g n i z e d by

subsequently described

d e s c r i b e d the mo ra in e

1958;

glacial

1915;

inner and o u t e r ridge

p.

302-

se pa ra te d b

flat o u tw a s h su rf a c es he n a me d the

M a n c e l o n a Plain.
A l t h o u g h p u b l i s h e d mo r e than 70 years ago,
L ev er et t
Martin,

and T a yl or
1955;

basic sour ce

maps by

(mapping later sli gh tl y m o d i f i e d by

and F a r r a n d and Bell,
for d e l i n e a t i n g glacia l

1982)

rem ai n the

features

Michigan.

T h e i r use of the term "moraine"

describing

the Port H u r o n feature

in

when

follows a c c e p t e d views

2

*
Huron v "
Moraine

Figure 1. T he Port Huron Moraine in southern Michigan
(after Leverett and Taylor, 1915).

of the time,

which placed

im po rt an ce of an ac ti v e
m o d e r n landscape.
ideas,

great em ph as is on the

ice m a r g i n

in pr o d u c i n g

the

M a r t i n ’s 1955 map pe r pe tu at ed these

as has F a r r a n d and B e l l ’s more recent m a p p i n g

(1982).

Certainly,

Le ve r e t t

and Tay lo r knew that glacial

s ta gn at io n o c c ur re d w i t h i n these morainic
from newly av a i l a bl e

large

scale

tracts.

topogra ph ic qu ad ran gle s

along with de ta i le d field mapping,

however,

st a g n a t i o n was m u c h more w i d e s p r e a d during
d e g l a c i a t i o n than p r e v i o u s l y recognized.
w a t e r and p e t r o l e u m well
p o s i t i v e r e la t io ns h ip s
topography,
Wi n t e r s

log da t a

(1979)

indicate that
final

In addition,

indicate strong

among drift thickness,

and m o d e r n terra in
documented

Data

bedrock

in some areas.

Ri ec k and

simila r rel at io ns hi ps

s o u t h e a s t e r n M i c h i g a n but no such study has

in

focused on

the no rt hw e s t er n pa r t of the So u t h e r n Peninsula.

Thus,

bo t h data and i n c r e a s e d u n d e r s t a n d i n g p r o v i d e a basis and
j u s t i f i c at i o n for r e e v a l u a t i n g

the Port H u r o n C o m p l e x

in

n o r t h w e s t - s o u t h e r n Michigan.
In addition,

the M a n c e l o n a P l a i n has long be e n

r e c o g n i z e d as an e s p e c i a l l y

impor tan t el eme nt

in the

int er pr e t a t i o n of the c o m p l i c a t e d pa t t e r n of mo ra i n ic
remnan ts

in this pa r t of the state

F a rr an d and Eschman,
has been limited.

1974),

(Melhorn,

1954;

but ana lysis of the

feature

T o p o g r a p h i c maps and aerial

p h o t o g r a p h s c l e a r l y show that the M a n c e l o n a P l a i n
a s s e m b l a g e of sever al
to the glacial margin,

is an

o u t w a s h te rr a c e s tr en din g pa ra lle l
yet the

relati ve age,

4

si g n i fi ca nc e,
th es e

co mpo s i ti on ,

fe at u r e s

an d Cobb,

and g e o g r a p h i c d i s t r i b u t i o n of

r e m a i n unknown.

1982)

in di c a t e

similar outwash surfaces

f l o w e d bo t h p a r a l l e l

the M a n c e l o n a

and aer ia l p h o t o g r a p h s also
previously undocumented,
to

the

terminus,
feature.

but no

and
suc h

study

T o p o g r a p h i c maps

sh o w that numerous,

outwash

su rfaces e xi st p r o x i m a l

Inner Port H u r o n Complex.

Problem
This
of

(Fraser

that m e l t w a t e r a s s o c i a t e d with

p e r p e n d i c u l a r to the gl aci al
has a d d r e s s e d

S t ud i e s e l s e w h e r e

research concerns

l a n df or ms and

st at em en t
the

nat ur e and s i g n i f i c a n c e

s e d i m e n t s w i t h i n Le ve r e t t an d T a y l o r ’s

In ne r and O u t e r Po r t H u r o n Mo ra ine s,
M a n c e l o n a Plain,

in n o r t h w e s t e r n

inclu din g

the

s o u t h e r n Mi c h i g a n .

The

m a j o r q u e s t i o n s a d d r e s s e d are:

1.
Wh a t e v i d e n c e ex i s t s for the p r e s e n c e of icec o n t a c t and p r o g l a c i a l s t r a t i f i e d sand and gravel, flow
and a b l a t i o n t i l l : and o t h e r s e di me nt i n d i c a t i v e of
s t a g n at io n ?
2.
To wh a t ex te n t does p r e s e n t t o p o g r a p h y d i s p l a y
m o r p h o l o g y ty pi c a l of s t a g n a n t ice f or mat io n?
3.
Wha t e v i d e n c e e x i s t s for the p r e s e n c e of
o u t w a s h s u r f a c e s w i t h i n the M a n c e l o n a Plain?

several

4.
Wha t e v i d e n c e e x i s t s for d r a i n a g e b o t h p a r a l l e l and
p e r p e n d i c u l a r to the ice m a r g i n on the M a n c e l o n a Plain?
5.
W h a t e v i d e n c e e x i s t s for the p r e s e n c e of o u t w a s h
su rf ac e s p r o x i m a l to the In ne r Port Hu ro n C o m p l e x ?
6.
To w h a t e x t e n t
modern topography?

does th e b e d r o c k s u rfa ce

influence

7.
Wh a t e v id e nc e exists in di ca ti ng that this po rti on
of the Port H u r o n C om p l e x for me d c. 13,000 yrs. B.P, as
su gg est ed in the li te ra tu re (Fullerton, 1980)?
In ad d i t i o n to e v a l u a t i n g
has two a d d i t i o n a l
1.

An

these

objectives

questions,

the study

of developing:

i m pr ov ed p h y s i o g r a p h y

for the st ud y area.

2.
An i n t e r p r e t a t i o n of de gl aciation,
lan dfo rm and sed ime nt relationships.

b a s e d on

B a c k g r o u n d and metho ds
D e f in it io ns

and con ce pt s - E a r l y workers,

p re va il in g vie ws

of the time,

relief to po g r a p h i c
as

"moraines."

trends

Flint

f o l l o wi ng

the

ma p pe d many of the high-

in n o r t h w e s t - s o u t h e r n Mi c h i g a n

(1971,

p.

199)

de f i n e d a m o r a i n e as

"an a c c u m u l a t i o n of drift d e p o s i t e d ch ief ly by dir ec t
glacial action,

and po ss e s s i n g

form ind ep en de nt
that mo r a i n e s

initial c o n s t r u c t i o n a l

of the floor be n e a t h it."

are

formed by act iv e

ice,

This

implies

and c o m p o s e d

p r i m a r i l y of till.
In contrast,

Kot ef f and Pessl

term " m o rp ho se qu en ce "

(1981,

and d e f i n e d

p.

5) c o i n e d the

it as "a c o n t i n u u m of

la ndforms co m p o s e d of m e l t w a t e r deposits,

from more

c o l l ap se d f or ms .. .t o p r o g r e s s i v e l y less c o l l a p s e d forms
downstream.
drift

It c a n. .. be v i e w e d as a body of

laid down,

layer up o n layer,

beyond the m a rg in of a glacier,

by m e l t w a t e r at and

whi le d e p o s i t i o n was

c o n t r o l l e d by a spe cif ic bas el ev el ."
concept,

w h i c h has p r o v e d use fu l

mar gin al p o s i t i o n s wh e r e
(Koteff,

1974),

st ra ti fe d

The m o r p h o s e q u e n c e

in d e t e r m i n i n g

ice

st ag na t i o n was p r e d o m i n a n t

is a p p l i c a b l e

in the

study area.

Koteff

6

(1974,

p.

121),

w h o uses the t e r m " m or ph ol og ic

in this early work,

pr ov ide s six cri te ri a

sequence"

for d e s i g n a t i o n

of m o r p h o s e q u e n c e s :
1.
M o r p h o s e q u e n c e s p r e d o m i n a n t l y consis t of me lt wat er
de po s i t s in c l u d i n g sand, gravel, silt, and clay.
Till is
us u a l l y absent e x c e p t where it a pp ea rs as flow till.
2.
M o r p h o s e q u e n c e s ge n e r a l l y show a t r a n s i t i o n from
more co l l a p s ed to less co l l a p s e d forms downstream.
3.
M o r p h o s e q u e n c e s are c o n t r o l l e d by a sp ecific base
level, us u a l l y i d e n t i f i a b l e in the field.
4.
L a n df or ms m a k i n g up a single m o r p h o s e q u e n c e are
co ns i d e re d to hav e formed at a p p r o x i m a t e l y the same time.
5.
S e d im en ts s h o w a t r a n s i t i o n from co a r s e to
texture d o w n s t r e a m from the head of outwash.

fine

6.
M o r p h o s e q u e n c e s can be d i s t i n g u i s h e d us ing profiles
dr awn p e r p e n d i c u l a r to the head of outwash, and, where
more than one m o r p h o s e q u e n c e is present, ex pr e s s a
s h i ng le -l ik e m o r p h o lo g y .
The g en es is

of m o r p h o s e q u e n c e s

la ndforms has b e e n d e s c r i b e d
Koteff and Pessl,

1981)

model of glac iat ion .
zone at the
glacier.

planes develop,
s up erg lac ial

depe ndi ng

using

the

sedim ent s

in the st a g n a n t zone

forming

on the p r o g l a c i a l

environment.

two

change

fine distally,

de po si te d near the

to

these

features

ice margin.

shear

to a
(Fig.

2).

se di me nt s

ou tw a s h apr on s or deltas

a ss oc ia te d w i t h th es e
from c o a r s e

retreat

ice i m m e d i a t e l y up-

w as t i n g tr a n s po rt

ice margin,

1974;

stagnation-zone

be tw ee n the two zones,

s u p p l y i n g basal

location

(Koteff,

This model assum es a th in stagnant

j un ct ur e

Me lt wa te r and ma s s
bey on d the

in det ai l

ice m a r g i n w i t h act iv e

At the

and t h e i r a s s o c i a t e d

exhibit

S e d i me nt s
a facies

with b o u l d e r s

FLOWTILL

ACTIVE ZONE
EROSIONAL SUPEP.GLACIAL STRE AM
SHEAR PLANES

BASAL SEDIMENTS ARE TRANSPORTED
TO SUPEP.GLACIAL POSITIONS

FLOWTILL MASS

^

‘

O U TW ASH.

,

FAN '----

STAGNANT
ZONE

*

h a n g in g valley

APRON

BOULDERS
FLOWTILL

H EA D O P
OUTWASH

DE POSITIONAL
FAN

SUPERGLACIAL STREAM
B U RIED ICE

ICE-CONTACT
SLOPE
g y /

(UPTOSOm)

SEDIME NTS)
SEOIMENTS)

V.E. b 300x

r-'L
I
C O ILA PS EO O U TW A SH

R EM N A N T O r
FO R M E R SURFACE

Figure 2. Landforms and sedim ents associated with a
stagnant ice margin (from Blewett, 1984).

8

The area al on g the

ice m a r g i n serves as the head of

o u t w a s h for the apron.

U p o n ablation,

ang le of repose

f o rm in g

Erosional

occurs,

va lle ys

an ice -c on ta ct

and a l l u v i a l

depositional

slope.

fans

are

along the h e a d of o u t w a s h as sup erg la ci al

m e l t w a t e r and se d i m e n t s are s l u i c e d
zone

to the

(which later b e c o m e h a ng in g v a l l e y s at

the hea d of outwash)
form ed

c ol la ps e

onto

the a p r o n

form w he re masses
In addition,

(Fig.

of

c re v as se

so that

eventually

As
the

and

re lat ed

the active
s t ag na nt

(major

delimiting

zone mi g r a t e s
la nd fo rm s

i c e- co nt ac t

f o rm er

features

ice b o u n d a r y

a series of st ag na t i o n

w i t h the heads of o u t w a s h
trends)

fil li ng s

zone.

re t r e a t s due to thinning,

r eg io na l

Kettles

st ag na nt

ice are b u r i e d by outwash.

form in the sta gn an t

accor din gly ,

2).

from the

still

rema in

slopes with

stands

of the

ice

margin.
B a s e d on e x t e n s i v e
Alaska,

studi es

Gu s t a v s o n and B o o t h r o y d

a l t e r n a t i v e model
meltwater

"fountai ns"

marking

Th e y q u e s t i o n the

of Koteff and Pessl

c o m p e l l i n g evi de nc e
s hea r plane s can
s up e r g l a c i a l

pr es en t an
in w h i c h

the d o w n s t r e a m ends of

and e n g l a c i a l

are p r o p o s e d as the p r i n c i p a l
dep osi tio n.

(1987)

of m o r p h o s e q u e n c e genes is

sediment-laden subglacial

model

of the M a l a s p i n a Glacier,

sou rc e

m e l t w a t e r streams

of gl a c i o f l u v i a l

stagnation-zone

in par t

be cau se

from the l i t e r a t u r e

1)

retrea t

there

to su gg e s t

s u p p l y large v o l u m e s of se d i m e n t

locations,

and

2)

the vo lu me s of

is no
that
to

s u p e r g l ac i al

d r i f t p r e s e n t on mos t

i n s u f f i c i e nt

to a c c o u n t

for the

gla cie rs

is

as so c i a t e d t h i c k ou tw as h

d e p o s i t s obse rv ed .
D e s pi t e u n c e r t a i n t i e s as to the g en es is
m o r p h o s e q u e n c e s , the
for a n a l y z i n g
w i t h the

c on ce pt p r o v i d e s a basis

t e r r a i n and s e d i m e n t s

associated

In ne r an d O u t e r Port H u r o n Complexes.

su pp o r t in g

its a p p l i c a t i o n

the ch ap te rs

Techniques

to

inte rpr et

in this

study

is p r o v i d e d

s tu dy uses

characteristics

of the r e g i o n to de scribe

m o r p h o s t r a t i g r a p h y , rock st ra t i g r a p h y,
by W i l l m a n and

R O C K S T R A T I G R A P H Y - Willman,

Swann,

"r o c k - s t r a t i g r a p h i c

significant

lithology

classification

lithologic

units have b e e n
states

ch ang es

is the
in the rock

see W i l l m a n and Frye,

f o rm al ly

identified

p r es en ts

detailed

lithologic

and I l l i n o i s

1970),

in Mi c h i ga n.

investigating

for the P l e i s t o c e n e

Indiana,

example,

a means of

for

A l t h o u g h rock st ra ti g r a p h i c

formally defined

su c h as Ohio,

5)

... The

that m a y be us e d to e s t a b l i s h a f r a m e w o r k

stratigraphic description."

ot her

p.

u n i t s are d e f i n e d and

o b j e c t i v e of r o c k - s t r a t i g r a p h i c
r e c o g n i t i o n of

and

Frye (1970).

and Frye (1958,

r e c o g n i z e d on the basis of o b s e r v a b l e

se qu enc e

in

the m o r p h o l o g i c and

time s t r a t i g r a p h y as d e f i n e d

state that

Ev id en ce

follow.

- Th i s

sedimentologic
and

of

none h a v e

The pr es e n t

d a t a on gl aci al

present

in

(for
been

st udy
deposits

t o p o g r a p h y and as a

as

10
foundation

for

fut ur e

rock-stratigraphic
are p r o v i d e d
textural

units.

but pr op o s e s

Methods

in the a p p e n d i c e s .

terms

th e i r g e ne ri c

research,

su c h as
sense,

"sand,"

of sed ime nt

Un l es s

Where specific

Wentworth classification
us e d

instead of

co n f u s i o n as to the

te rms

are i n t e n d e d the
The t e r m

is i d e n t i f i ed p r i m a r i l y

un i t

from the

Frye
as

(1970,

from c o n t i g u o u s units;

surface

its ex te n t . "

the

ext en t

This

s t u d y and

form it

scale)

lithologically

in n o r t h w e s t e r n

c o n s t i t u t e d an

(1981)

ice m a r g i n a l

s o u t h e r n Michigan.
(1:24,000

c l a s s i f i c a t i o n.
an a l y z e d e t a i l s

and

im portant part of this

i n c l u d e d c o n s t r u c t i o n of to po g r a p h i c

t r a c i n g of contours,

time

and T a y l o r ’s Port H u r o n

Detailed topographic map analysis
1: 25,000

43)

r e s e a r c h uses m o r p h o l o g i c

of nine p r i n c i p a l

positions within Leverett
Mo r a i n i c C o m p l e x

p.

it m a y or ma y not t r a n s g r e s s

c r i t e r i a as d e s c r i b e d by K o t e f f and Pessl
to define

and p r e l i m i n a r y

profiles,

landform

A e r i a l p h o t o g r a p h y was also u s e d to
of the

lo ca ti ng expos ur es .

is

"a body of ro c k that

it m a y or m a y not be d i s t i n c t i v e

throughout

"till"

i n t e r p r e t a t i o n of these deposits.

a morphostratigraphic

displays;

in

in order to a v o i d an y

M O R P H O S T R A T I G R A P H Y - W i l l m a n and
de fi n e

are us e d

of A g r i c u l t u r e

is employed.

"d i a m i c t on "

etc.

in a c c o r d a n c e w i t h the

W e n t w o r t h c l a s s i f i c a t i o n or U.S Dept,
ter mi nology.

ana ly si s

o t h e r w i s e noted,

"gravel,"

r a t h e r th a n

no formal

landscape

and as an aid

in

F i e l d o b s e r v a t i o n s were ma d e

from

11
p as sa b le

roads and on foot.

m a p p a b le units,
d e f i n ab le

All were used

in d e li n e a t i n g

w h i c h are d e f i n e d as la ndforms w i t h a

set of g e o m o r p h i c

cha rac ter ist ic s.

TIME S T R A T I G R A P H Y - A t i m e - s t r a t i g r a p h i c unit

is define d

as a " s u b d i v i s i o n of rocks c o n s i d e r e d solely as a record
of a sp ecific
657).

interval of time"

(A.C.S.N.

Code,

R a d i o c a r b o n dates are u s e d e x te n s i v e l y

establishing

t i m e - s t r a t i g r a p h i c units

of the Pl ei stocene,

and this

on organic ma te r i a l

from s e p a r a t e

1961;

p.

in

for the latest part

r e s e a r c h pr esents

two dates

lo cations w i t h i n the

Inner and O u t e r Port H u r o n Complexes.

S t u d y area
The study ar e a
Charlevoix,
km.2

in cludes p a r t s

and O t s e g o Co unties,

of Kalkaska,

and c o n t a i n s about

As ma pp e d by L e v e r e t t an d T a y l o r

and O u t e r Port H u r o n fe at ur es
south we st

in p a r a l l e l

Antrim,

(1915),

the

1,900

Inner

tr en d g e n e r a l l y no rt h e a s t -

f a s h i o n acr os s the region,

se p a r a t e d by the Maxiceloxia P l a i n
R e i n t e r p r e t a t i o n of these

(Fig.

fe at ur es

3).
requires

a

m o d i f i c a t i o n of L e v e r e t t and T a y l o r ’s m a j o r l a n d f o r m
groupings.

Four p r i n c i p a l

are r e c o g n i z e d

p h y s i o g r a p h i c units

in the p r e s e n t

(Fig.

study:

1.

Inner Port H u r o n C o m p l e x
M a n c e l o n a Plain)

2.

Post

3.

O u t e r Port H u r o n C o m p l e x

4.

Flu te d U pl an ds

(including

Inner Po r t H u r o n zone

and T h r o u g h Va lle ys

the

4)

12

R 4W
MORAINES

OUTWASH AND
GLACIAL CHANNELS

i'V ' 1

LAKE BEDS, SAND

T 32 N

R 5W
T 31 N

GROUND MORAINES

» *-

R 6W
T 30 N

R 7W
T 29 N

RiW
T 28 N

T 27 N
10 km
10

T 26 N

A rea
sh o w n
above

T 25 N

►

k

i

J

Figure 3. Major landform groups
a s m apped by Martin (1955).

ml

13

INNER PORT
HURON COMPLEX

I w

R 4W
'« >

PO ST INNER PORT
HURON ZONE

4J

T 32 N

FLUTED UPLANDS AND
THROUGH VALLEYS

R 5W
T 31 N

\ittw'*
’•ro>;ns

OUTER PORT
HURON COMPLEX

R 6W

i,,v*V*T

T 30 N

SftsW&iiSBflr

R 7W
T 29 N

R 8W

5®$3&s
m m
T 28 N
ICE-MARGINAL
POSITIONS

sag s®
T 27 N

10

mm
m

&

m

m

10 Km
mi

1

,

|Pvi

T 26 N

A re a
sh o w n
above

s '
T 25 N

X

'

Figure 4. Major landform groups recognized in this study

14
In the c h a p t e r s

to

follow,

these

regions

are d i s c u s e e d

in the o rd er gi ven above.

The

is d i s c u s s e d

first be c a u s e

it

this

The c l o s e l y a s s o c i a t e d Post Port H u r o n

study.

is p r e s e n t e d next,
Complex.

D et ai ls

Fl ut e d u p l a n d s
discussed

Inner Port H u r o n C o mp le x
is of c en tra l

im po rt an ce to
zone

fol lo we d by the O u t e r Port H u ro n
of each are p r o v i d e d

in C h a p t e r

and a s s o c i a t e d t h ro u g h v a l l e y s

separately because

3.

are not

they are a n c i l l a r y

to the

study.

Literature
Taylor
continuous

(1897)

mapped

feature,

(1899,

for the first

the Port H u r o n C o m p l e x as a

paralleling

Port H u r o n to the Au
Taylor

review

Plate

the Lake H u r o n coast

Sable River.
II)

In a la ter work,

correlated

time w i t h m o r a i n e s

from

the Port H u r o n Mo rai ne

in n o r t h w e s t e r n sou th er n

Michigan.
Ba sed on these and ot he r
(idlo)

m a p p e d the m o r a i n e

n o r t h e r n par t
t ra c e d the

of the

feature

studies,

Leverett

in a br oa d arc a c r o s s

Southern Peninsula

to Muskegon,

moraines

in e a s t e r n W is con si n.

younger,

p ro xi m al

morainic

and T a y l o r

(Fig.

and c o r r e l a t e d

the

1).

They

it wi th

A c l o s e l y ass oc iat ed,

system,

the M a n is te e,

was

ju dg ed c o r r e l a t i v e w i t h l a n d f o r m s c o m p o s e d of red till
n o r t h e a s t e r n Wiscons in.
Le v e r e t t

and T a y l o r b e l i e v e d that the Po rt H u r o n

Complex marked a readvance
in ter pre tat ion ,

which

of the

is still

ice.

ac ce p t e d

but

This
(Harrow and

in

15
Calkin,
lake,

1985),

p o s t u l a t e d that

Lake Arkona,

a lo w - a l t i t u d e

o c c u p i e d the

glaci al

s o u t h e r n sec ti on s of the

Lake H u r o n b a s i n p r i o r to f o r m a t i o n of the Port H u r o n
Moraine.

Advance

of Port H u r o n

the w a te r s of Lake A r k o n a and
al t i t u d e

lake,

t r u n c a t i o n of Lake A r k o n a b e a c h

w i t h the Port

Huron

p o s t u l a t e d that

documented

fe at u r e s by the mo rai ne

s o u t h e r n Mi chigan,

the p a r a l l e l

in time

d e s c r i p t i o n s of

nature

(1915,

p.

303).

Compared

featu re

short.

formations

Port H u r o n M o r a i n e

of the I nn er and

to

elsewhere

L e v e r e t t ’s n a r r a t i v e

is q u i t e

m a p of su r f i c i a l

Le ve ret t

i n d i c a t e d a ra th e r close

the Port H u r o n

however,

of the m or a i n e

(1905)

feature.

O u t e r Port H u r o n M o r a i n e s

Michigan,

Taylor

higher

Lake W h i t t l e s e y was p e n e c o n t e m p o r a n e o u s

In n o r t h w e s t e r n

relationship

into the b a s i n pon de d

formed a new,

Lake Wh it t l e s e y .

and show ed that

ice

on thi s

in
sectio n

L e v e r e t t also p u b l i s h e d a

in 1924

that

i n c l u d e d the

(though it was e s s e n t i a l l y u n c h a n g e d

from pr ev i o u s

maps),

the s u r fi ci al

g e o l o g y of A n t r i m and C h a r l e v o i x Cou nt ie s

(1925a,

studied glacial

southern Michigan
1953;

(Bergquist,

noted

well

indurated,

the p r e s e n c e

some places.

deposits
1938,

B e r g q u i s t and Zinn,

b e l i e v e d that Port H u r o n till
jointed,

short r e po rt s on

1925b).

Bergquist

1952,

and c o m p l e t e d two

in n o r t h w e s t e r n

1940,

1944a,

1945,

1944b),

1946,
and

c o v e r e d an older,

hi g h l y

c h o c o l a t e - c o l o r e d clay.

of red till atop Port H u r o n

He also

till

in

16

Subsequent
fo l l o w s
buried
Two

georaorphic s t u d y

in n o r t h e r n M i c h i g a n

i n t e r p r e t a t i o n s b a s e d on W i s c o n s i n ’s Two Creeks
forest

Creeks

(Chamberlin,

site co n s i s t s

upward

into

lacustrine

g r ad e s

into l a c u s t r i n e

a s s o c i a t e d wi t h this

1906;

Thwaites,

of a r e d - g r a y till

sand an d clay,
sand.

the

forest

and Farrand,

1963).

w i t h Va ld e r s

till,

Valders Quarry

11,850

recognized

site

G l e n w o o d and C a l u m e t

be ac he s

shorelin es.

there

east-west

at

is just n o r t h of

n o t e d the t e r m i n a t i o n of
by a moraine.

relationships
till ab ove

a r e a d v a n c e w as proposed.

of this

till

He c o r r e l a t e d
in

is a s i m i l a r t e r m i n a t i o n of rais ed

a p p a r e n t p o s i t i o n of Va l d e r s

terminus

(Broeker

39 km southwest.

L e v e r e t t ’s M a n i s t e e M o r a i n e

B a s e d on these

at Two Creeks,

B.P.

till was c o r r e l a t e d

in W i s c o n s i n

(1918)

where

is

by ice w h i c h

as the u p p e r m o s t

1943),

the are a wh er e A l d e n

M ic h ig an,

forest

± 100 yrs.

This o v e r l y i n g

(Thwaites,

this mo ra i n e w i t h

in turn

sand and o v e r l a i n by a red cl a y till

c.

The Two C r ee ks

The

gr a d i n g

which,

Th e b u r i e d

i n t e r p r e t e d as h a v i n g been d e p o s i t e d
overrode

1943).

advance,

named

and the

the b u r i e d
The

the Valders,

line c o n n e c t i n g M a n i s t e e

forest

so u t h w a r d
lies on an

and Two Creeks,

Wisconsin.
In Michigan,
found,

yet

no b u ri ed

in m a n y p l a c e s

forest of c o m p a r a b l e

red till ove rl ie s

a b r o w n till,

s i m i l a r to the s t r a t i g r a p h y at the Two Cre ek s
Based

on this evi dence,

pl us

age was

site.

the t e r m i n a t i o n of raised

17
shore lin es

by the M a n i s t e e Moraine,

red till was c o r r e l a t e d w i t h
Creeks.

the V a ld er s till at Two

It was on this basis that the V a l d e r s

was rec og n iz ed

(informally)

in M i c h i g a n

In r e c o n n a i s s a n c e m a p p i n g
shore,

n o r t h e r n M i c h i g a n ’s

Brets

Muskegon,

(1951)

(Bretz,

1951).

along the Lake M i c h i g a n

tra ce d red till

and e xt en d ed the V a l d e r s

He p o st ul a te d that Va ld e r s

rea dvance

s o ut hw ard to
limit to this point.

ice ov errode

Port H u r o n advance and p l a s t e r e d

mo ra in es

red till

of the

on top of these

ea rl ie r deposits.
M el ho r n

(1954)

m a p p e d the extent of Va l d e r s

nor t h e r n M i c h i g a n on the a s s u m p t i o n that
hue that would d i s t i n g u i s h
However,

(Farrand,

1976).

diminished

that Port H u r o n

it had a reddi sh

in importance

till m a y also be red

Like Bretz b e f o r e him,

that red till of the V a l d e r s
H u r o n till.

in

it from brown Port H u r o n till.

this wo rk has since

wi t h the r e c o g n i t i o n

drift

M e l h o r n be li e v e d

read va nc e o v e r l a i d Port

He p o s t u l a t e d that V a ld er s

o b s t r u c t e d by the high bl uf f s

of

the

ice was

Port

Hu r o n C o mp le x

and that a thin layer of red till was d e p o s i t e d atop Port
H u r o n sediments,
Me l h o r n did
tills

especially

indeed d i s c o v e r

(Port H u r o n drift)

was unable to d e m o n s t r a t e

in areas of lower elevation.
red tills ov e r l y i n g b ro wn

in n o r t h e a s t e r n Michigan,
similar associations

but he

in the

presen t study area.
Melhorn,
Huron

in d e s cr i b i n g

features,

places,

indi ca te s

are co mp os ed

the

that

Inner and O u t e r Port
the ridges,

of s t r a t i f i e d drift,

at least
incl ud in g

in
ice-

18

co nta ct deposits.
level

l a c us t ri ne

outer

feature.

He also

r ep or ts

the p r e s e n c e

sedim en ts along proxim al

A ye a r l at er M a r t i n ’s (1955)

L e v e r e t t ’s e a r l i e r map,
cartographic

source

sections of the

surficial

of the S o u t h e r n P e n i n su la was published.

of high-

g e ol o g y map

A re vi s i on of

it se r ve d as the basic

for n e a r l y

30 years.

M a r t i n also

p u b l i s h e d a short p op u l a r g e o l o g y of Grand Tr av er se
County

(Martin,

By
Huron

1960,

1957).

r ad io c a r b o n dat in g

re ad va n ce

(Suess,

B a r e n d s e n et a l ., 1957;
on these dates,

1954;

had c o n fi rm ed

Flint and Rubin,

Hough,

1958)

the Port
1955;

in Ontario.

Based

H o u g h as s i g n e d an age of 13,000 yrs.

B.P.

to the Port H u r o n event.
R e s e a r c h since

1960 has

and s i g n i f i c a n c e of Valde rs
ol der d e p o s i t s

f o c u s e d p r i m a r i l y on the age
till and

its r e l a t i o n to

in n o r t h e r n M i c h i g a n and Wisconsin.

Interpretations

are c o m p l i c a t e d and still unresolved.

Ma jo r p r o p o s a l s

and c o m p l i c a t i n g

factors are re vi ew ed

below:
1.
A b ur i e d br y o p h yt e bed nea r Ch e b o y g a n a p pa re nt ly
ma rk s an ic e-f ree interval 13,000 - 12,500 yrs. B.P.,
befor e the Port H u r o n r e a d v a n c e (Cary-Port H u r o n
interstade, Fa r r a n d et a l ., 1969).
A single red till
above this de p o si t ind ic ate s that the ice front did not
r e tr ea t a p p r e c i a b l y du r in g the Two Cree ks interstade
(Farrand et a l ., 1969).
F u l l e r t o n (1980) que st ion s
this i n t e r p r e t a t i o n and c o r r e l a t e s the bry op hy te bed
w i t h the Two Cre ek s bu r ie d forest.
2.
A c c o r d i n g to E v en so n and M i c k e l s o n (1974), the type
V a l d e r s till (Thwaites, 1943) at V a lde rs Q u a r r y
c o r r e l a t e s w i t h the till beneath, rather than above,
the Two C r e e k s forest. If true, Valders till is not

19
V a ld er a n in age.
E v e n s o n e t . a l . (1976) p r o p o s e the
name "G rea tla kea n" as a r e p la ce me nt for the advan ce
burying the Two C r e e k s forest.
3.
Based on a n a l y s i s of s h o r e l i n e s and glacial
deposits, E v e n s o n (1973) q u e s t i o n e d B r e t z ’s
notio n of a V a l d e r s re a d v a n c e as far south as Muskegon.
He ma i n t a i ns that s h o re li ne r e la ti on sh ip s and
co rr e l at io n s d e s c r i b e d by Le ve re tt and T a y l o r and by
Ald en are e s s e n t i a l l y accurate.
If true, this limits
the V a l d e r s / G r e a t l a k e a n a d v a n c e to the ar e a n o r t h of
the M a n i s t e e - T w o C r e e k s line.
4.
Both Port H u r o n and G r e a t l a k e a n tills in
n o r t h w e s t e r n M i c h i g a n are red in color and show similar
clay m i n e r o l o g y (Farrand, 1976; Monaghan, 1988); the
red till b o u n d a r y ma p p e d by M e l h o r n (1954) is pro bab ly
incorrect.
5.
Li ne b e c k et. a l . (1974) co r r e l a t e the I nn er and
Ou te r Port H u r o n M o r a i n e s w i t h W i s c o n s i n ’s Sh o r e w o o d
and Ma n i t o w o c tills, respectively.
In M i c h i g a n Ta 3rlor
(1979, 1981) r e la te s O r c h a r d Lake till to the Port
Huron read va nc e and Filer till to the Grea tl ak ea n.
These studies are an attem pt to e s t a b l i s h rockst ra ti gr ap hi c c r i t e r i a for Inner and O u t e r Port 'Huron
deposits.
Burgis

(1977)

p r o p o s e d the term

M i c h i g a n ’s e q u i v a l e n t
Many la ndforms

features,
events

and she

are p o s s i b l e

Inner and Ou te r Port H u r o n

study area as they rel at e

de po s i t s

(1982)

to

p u b l i s h e d a map of the

of the S o u t h e r n Peninsula.

and O ut er Port H u r o n C o m p l e x e s
mor aines of c o a r s e - t e x t u r e d
nea r l y

stadial.

in n o r t h e a s t e r n s o u t h e r n Michigan.

Farrand an d Bell
surficial

for

includes a short d i s c u s s i o n of cutwach

in the p r e s e n t

dra in ag e

to the V a l d e r s / G r e a t l a k e a n

s t u d i e d by Bu rg i s

co rr e l a t i v e s w i t h the

"Onaw ay advanc e"

identical

Winters,

to M a r t i n

Rieck,

ch a r a c t e r i s t i c s

are ma pp e d as

till,"

The

Inner

"end

and b o u n d a r i e s

are

(1955).

and Ka p p

(1986)

described

of m i d - W i s c o n s i n a n organ ic d e p o s i t s

rec o rd e d

fr om we lls

drilled

in the M a n c e l o n a P la in

(details of s t r a t i g r a p h y are d i s c u s s e d
They state

(p.

296)

that

in C h a p t e r

"the O u t e r Port H u r o n Morain e

co ns is ts m a i n l y of se d i m e n t s

associated with a

o u t w a s h ’ ..."

Likewise,

note

Inner and O u t e r Port H u r o n

that

the

A n d e r s o n and R i e c k

co m p o s e d of g l a c i o f l u v i a l
mor ai ne s

composed

sediments

st udi es

th ere

as to the c h a r a c t e r

in the st ud y area.
c o r r e l a t i o n . age,
re l a t i o n s h i p s

p r i m a r i l y of g l a c i o f l u v i a l
to as a " s a n d u r . "

varies,

of the word,
Sand ar have
sandar"

end

the c o m p o s i t i o n ,

This

degrees,

sediments,

it ca n be ref erred

term has

been d i v i d e d

(Krigstrom,

associated with

denotes

into

1962).

n or ma ll y has been c a l l e d

long been used

T h o u g h sp el l i n g of

"sandar"

precise

the M a n c e l o n a P l a i n consist s

is g e n e r a l l y used as the

wh il e

qu es tionable.

that e s t a b l i s h e s

Icelandic

depo sit ion .

in n o r t h w e s t e r n

relat ion shi ps.

certain landforms

"sandur"

are

of the Port H u r o n Compl exe s

to va ry i n g

stratigraphic

glaciofluvial

fe at u r e s

and are not

of the Port H u r o n C o m p l e x

san da r - Be ca u s e

to d e s c r i b e

brief ly

s i g n i f i c a n c e , and d e t a i l e d

No d e t a i l e d wo r k has be e n done

R ev i e w of

(1987)

is c o n s i d e r a b l e

S i m p l y stated,

s ou t h er n M i c h i g a n are

l an d f or m and

’head of

of till.

Fr om all these
c o n f us io n

2).

the term

singular

the p l u r a l

" v al le y sandar"

In N o r t h A m e r i c a

"v al le y train"

while

form

form.
and

the
the

"plain
former
latter

21
has be e n r e f er re d

to as

"o u t w a s h apron"

or "o ut w a sh

p l a i n . ’’
Major research
presently
and

experiencing

include w or ks

(1969),

on sa n d u r p r o c e s s e s

Rust

Gustavson

(1974),

Church

1983),

Rust

have

(1978)

is n o t e w o r t h y due

types)

(1978).

to

associations

(Miall,

1985),

interpreting glaciofluvial
in cl u d e s

inese g i a c i u l u g x c a l
sand ar

Donjek,

Platte

environmental

r e m a i n us ef u l

environments.

in

The s t u d y by
cov erage

and m o r p ho lo gy .
s t ud ie s

in areas

are use fu l

of P l e i s t o c e n e

s o u t h e r n Michigan.

the p r o c e s s - o r i e n t e d

studies

to the

1978,

been s u p e r s e d e d by

such as n o r t h w e s t e r n

parallel

(1977,

a d e t a i l e d and e x h a u s t i v e

of b o t h sa n d a r p r o c e s s e s

interpreting

and

of c h a r a c t e r i s t i c

specif ic

have

th e y

1979),

M i a l l ’s 1983 work

(Scott,

for d e l i n e a t i n g

later w o r k

(1972)

by M ia ll

(1979).

ideas

and Rust

(1974,

(1975)

few,

Sedimentological

its d e v e l o p m e n t

T h o u g h these

Williams

Bl uc k

been d e s c r i b e d

settings.

Church

(1972),

and B l u c k

sediment/structure
and Slims

(1963),

B o o t h r o y d and A s h l e y

B o o t h r o y d and N u m m e d a l
characteristics

g l a c i a t i o n are c o m p a r a t i v e l y

by F a h n e s t o c k

(1972),

in areas

involve

for
glaciation

Ho wever,

sa nd a r

few of

formed

ice m a r g i n s u c h as the M a n c e l o n a Plain.

Justification
Interpretations

of the m o r p h o l o g y and g e n e s i s

of the

Port H u r o n C o m p l e x are b as ed p r i m a r i l y on the d a t e d wo r k
of M e l h o r n

(1954)

and L e v e r e t t

and T a y l o r

(1915).

22
F a r r a n d and B e l l ’s (1982)
as

rece nt ma ppi ng of the feature

"end morain e of c o a r s e - t e x t u r e d till"

pa t t e r n s

ne ar l y

identical

to M a r t i n

uses areal

(1955;

in turn based

on Lev erett and Taylor).
Recent

field w o r k and n e w l y avai la bl e

t o p og ra ph ic maps

indicate

co m p l i c a t e d a s s e m b l a g e
m a r g i n a l l y stagnant,
g lac io flu vi al
co m p o n en t
Indeed,

c o n ta i n

ice and that

by far the most

of the present

gravel pits

important

topography.

in the most p r o x im al

sections

(mapped as m o r a i n e by Lev ere tt and

st ra ti f i e d

of 8 met er s or more,
di s p l a y the typic al

formed along

rat he r than active,

in d e v e l o p m e n t

of the inner ridge

the area is co mp o s ed of a

of la n d f o r m s

d e p o s i t i o n was

several

Taylor)

that

large-scale

while

sand and

gravels to a depth

to p o g r a p h i c map co ntours

bowed p a t t e r n a s so ci a t e d wi t h outwash

aprons.
R.J.

Price

(1973,

p.

19)

has

stated:

T he re is no excuse for those a ut hor s who insist
on ca l l i n g a ridge or a series of m o u n d s of well
sorted s t r a t i f i e d sand an d gravel a moraine, when
there is a b u n d a n t e v i d en ce that m e l t w a t e r rather
than ice is p r i m a r i l y r e s p o n s i b l e for its
deposition.

T h o u g h Price wa s m a i n l y c o n c e r n e d w i t h
terminology,

his w o r d s

em p h a s i z e

the need

u n d e r s t a n d i n g of l a n d f o r m ge n e s i s
using

"end mo ra in e"

g l a c i o fl uv ia l

to d e s c r i b e

sediments.

for a tho rough

and the da n g e r s

of

features c o m p o s e d of

Abundant

that the Port H u r o n Mo ra i n e s

in ap p r o p r i a t e

ev id enc e

in dicates

are not w h o l l y the product

23
of act iv e

ice d e p o s i t i o n and are not c o m p o s e d l a r g e l y of

till as the te r m "moraine"

implies.

bas ed on more m o d e r n co nc e p t s

Additional

study,

of glacial g e o m o r p h o l o g y is

needed.
A lo ng w i t h
inv es t i g a t e s

l a n d f o rm genes is and mapping,

this

study

the d e g l a c i a t i o n hi st o r y of n o r t h w e s t e r n

s o u t h e r n Michigan.

F a rr an d and Es c h m an

(1974,

p.

46)

state:
...the key to u n r a v e l l i n g the t an gl ed mess of mo ra ini c
remnants in this area, and w o r k i n g out the d e t a i l s of
the series of ice-fro nt al p o s i t i o n s du r i n g r e t r e a t from
the O u t e r Port Huron, is found in the series of well
d e v e l o p e d o u t w a s h surfaces that repr es en t the v a ri ou s
m e l t w a t e r d r a i n a g e w a y s , ea c h of w hi ch is g r a d e d from a
mo r a i n e u l t i m a t e l y to a p r o g l a c i a l lake stage in one of
the b o r d e r i n g lake basins, to the west or east.
A
careful m a p p i n g of these d r a i n a g e w a y s u si ng
ge om or p h o l o g y, lithology, and stratigraphy, will, we
believe, e v e n t u a l l y give us the ice frontal sequence.

At the ve r y least,

this study pr ov i d e s a so li d f o un da t i o n

for f o l lo w- up w o r k on m o r a i n e s an d o u t w a s h su r f a c e s
the n o r t h w e s t e r n part of the S o u t h e r n Pe ninsula.
important,

it reveals,

mo rp ho lo gi c,

for the first time,

u n d e r s t a n d i n g of g l ac ia l and p o s t - g l a c i a l
part of Michigan.

More

detailed

s t r a t i g r a p h i c , and ch r o n o l o g i c

w i t h i n the Port H u r o n C o m p l e x and pr ov i d e s

in

relationships
an im pr ov ed

events

in this

Ch a p t e r

2

PA L E O Z O I C B E D R O C K AN D Q U A T E R N A R Y SE D I M E N T S A S S O C I A T E D WITH
T HE IN NER AN D O U T E R PORT HU RO N COMPLEXES:
REVI EW AND NEW FINDINGS

B E D R O C K GE OL OG Y
Paleozoic
(1936),

Lan de s and Ehlers

Milstein
(Fig.

s ed i m e n t a r y rocks,

(1987),

5).

(1945),

d e s c r i b e d by M a r t i n
Fi sc he r

un d e r l y th ic k drift

S u bc ro pp in g

(1969),

in the

and

study area

li t h o l o g y co ns i s ts p r i m a r i l y of

the t r a n s i t o r y E l l s w o r t h and A n t r i m f or ma ti on s of the
D e v o n i a n an d M i s s i s s i p p i a n pe rio ds and the M i s s i s s i p p i a n
C o l d w a t e r and Ma rs h al l
dips

formations.

R e g i o n a l l y ea c h unit

s o u t h e a s t w a r d tow ar d the c e nt er of the M i c h i g a n

st ru ct u r a l

basin;

structure,

The E l l s w o r t h a n d
Traverse

group

may vary

locally.

An't.-rim fo rm at io ns ov er li e the

(Devonian)

s t r a t i g r a p h i c position,

however,

and ac t u a l l y o c c u p y the

their d i f f e r e n c e s be ing

p ro d u c t of a facies change.

same

the

E l l s w o r t h Shale exis ts

n o r t h w e s t e r n s o ut he rn M i c h i g a n and

is a soft,

in

semi­

in du ra te d gr ee n shale wi t h bands of ca lc a r e o u s material.
The t h i n - b e d d e d and

fissile A n t r i m Shale

is lo c a t ed

n o r t h e a s t e r n so u t h e r n M i c h i g a n and con si st s
brown,

in

of cinna mon -

d a r k g r a y - b l a c k shale wi th no du le s of li me sto ne

and pyrite.

El l s w o r t h Sh ale crops
24

out at se ve ra l places

25

Antrim
Shale

CHARLEVOIXCO.
.ANTRIMCO. * 1

Sunbury

Sandstone

C
M U M

•

mmmmm m M M

: OTSEGO CO.
• M M

•

B' KALKASKACO. J CRAWFORD CO.
Coldwater! Shale

Marshall
Sandstone

Figure 5. Bedrock g eo lo g y (from Milstein, 1987),
show ing the relationship with the Inner and Outer
Port Huron C om plexes.

26

in w e s t e r n A n t r i m a n d s o u t h e r n C h a r l e v o i x counties;
type s ec t i o n

is

in the E l l s w o r t h Quarry.

The o v e r l y i n g C o l d w a t e r S h a l e and M a r s h a l l
are not e x p o s e d
wells,

light

in the s t u d y area.

Coldwater

scattered

S ha le

Where

is v a r i a b l e

s a n d y lenses.

gray to w h i t e

(Melhorn,

its

Marshall

Sandstone

r e a c h e d by

in col or and c o nt ai ns
Sa nd st on e c o n s i s t s

of

sa n d s t o n e w i t h shale p a r t i n g s

1954 ) .

Al tog et her ,

these

rocks h e l p def in e

b o u n d a r y of Q u a t e r n a r y d e p o s i t s
Characteristics

the

l o we r

in the stu dy area.

of the b e d r o c k s u rf ac e and

its r e l a t i o n

to t o p o g r a p h y are d i s c u s s e d below.

BEDROCK SURFACE
Re c e n t l y c o m p i l e d but u n p u b l i s h e d maps of b e d r o c k
t o p o g r a p h y for Antrim,
C o u n t i e s were
use

in this

Ch ar lev oix ,

Otsego,

g e n e r o u s l y p r o v i d e d by Dr.

study

R i e c k for

1:63,360

scale;

B a s e d on an e x a m i n a t i o n of t h o u s a n d s

of well

logs,

th es e map s

bedrock

i n f o r m a t i o n now av ailable,

for r e g i o n a l i z i n g

R.L.

(Rieck,. v a r i o u s dates;

50 foot co nto urs ).

and K a l k a s k a

f u r n i s h the most d e t a i l e d

its surface.

d a t a are p r e s e n t e d

in feet

and p r o v i d e

a basis

In the d i s c u s s i o n s

in o rd er

be low

to m a t c h F i g u r e

6.

Bedrock topography
The u n d ul at in g,
b e d r o c k s ur f a c e
f o l l ow in g

high relief

(Fig.

(500-800

6) ca n be d i vi de d

four sections:

by i n t e r c o n n e c t e d v a l l e y s

ft,

15 0 - 2 4 5 m)

into the

1) e l l i p t i c a l u p l a n d s
in e a s t - c e n t r a l

separated

Charlevoix

27

RBW

R 7W

R 6W

R 5W

R4W
T 33 N

H.
Charievoix County
O tsego County

Antrim County

T 32 N

T 31 N

CHARLEVOIX
VALLEY
T 30 N
+ contours shown In last

500--- 1
450

black areas delimit princpal
bedrock valleys

VALLEY

«o

T 29 N

550

Antnm County
» * « • • M* • ee

T 28 N

Kalkaska County

T 27 N
d a r r ’a g h

VALLEY BSn

T 28 N

)\

KALKASKA
VALLEY
T 25 N

Figure 6. Bedrock topography (© 1 9 8 1 ,
1985, R.L. Rieck; used with perm ission).

28

County,
reg i o n

2)

a relatively high altitude

in e x t r e m e

lowlands east

p l a t e a u - l i k e tract,

ab ou t

punctuated

li n e a r v a l l e y s

ft,

305 m)

s o u t h e a s t e r n C h a r l e v o i x County,

east-west trending

altitude,

(1000

of A l b a and,

6 5 0-7 00

ft

4)

a

(200-215 m)

by northwest-southeast

3)

in

trending

in K a l k a s k a County.
Bedrock valleys

Four notable
Kalkaska,

b e d r o c k va ll ey s,

Darragh,

Alba,

buried beneath drift

and C h a r l e v o i x valleys,

in the

s t u d y area.

is o r i e n t e d n o r t h w e s t - s o u t h e a s t
principally
345

ft

exceed

in T.

(105 m)
600

Valley,

ft

27

N.,

which

R.

an d

7 W.

below adjacent
(180 m)

i n f o r m a l l y n a m e d the

T h a l w e g d e p t h av er age s

b e d r o c k u p l a n d s but may

t o w a r d the no rthwest.

is r e l a t i v e l y shallow,

averages

The

Al b a V a l l e y
30 N , , R.
(45 m)

(40 m)

straddles

5 W.

deep.

an d T.

R.

7 W.

east-west

and
oriented

the A n t r i m - Q t s e g o C o u n t y line
30 N . , R.

4W.

and is a b o u t

in T.

150

ft

Charlevoix Valley trends northwest-

s o u t h e a s t a c r o s s T.
the

in depth.

Darragh

tren ds e a s t - w e s t

27 N.,

ft

Kalkaska Valley

is l o c a t e d

a l o n g the n o r t h e r n b o u n d a r y of T.
130

lie

32 N.,

R.

5 W.

a n d is a s s o c i a t e d w i t h

i n t e r c o n n e c t e d v a l l e y s a n d e l l i p t i c a l u p l a n d s al r e a d y

described.
R i e c k and W i n t e r s

(1979)

bedrock lowlands elsewhere
preglacial
valleys

s t r e a m va lleys.

in the p r e s e n t

attributed buried

line ar

in M i c h i g a n to m o d i f i e d
P a t t e r n and f o r m of b e d r o c k

s t u d y s u gg e s t

a s i m i l a r genesis.

29
Regional,

p r e g l a c i a l dr ai n a g e p a t t e r n s here ha v e

be de te r m i n e d due
points,

yet to

to 1) the u n e v e n d i s t r i b u t i o n of data

2) p a u c i t y of tr i b u t a r y va ll ey s that mi gh t

indicate

flow direction,

and 3) the u n k n o w n a m o u n t

glacial m o d i f i c a t i o n that has occurred.

Reconstructions

of pr eg l a c i a l d r a i n a g e el s e w h e r e by other w o r k e r s
and Eschman,

1971)

syst em in what

p o s t u l a t e a m a j o r no rth fl ow in g

to the n o r t h w e s t

Evi d e nc e s u p p o r t i n g

be d r o c k v al le y s

Antrim,

river

in the s tu dy area.

this c o n c l u s i o n

that b e c o m e s

direction.

(Dorr

is now the Lake M i c h i g a n b a s i n that

favore d d ra i n a g e

surface

of

includes

a bedrock

lower tow ar d the northwest,

that tend to d e e p e n

Thus,

1)

in the

and 2)

same

p r e gl ac ia l st re am s

in w e s t e r n Kalkaska,

and C h a r l e v o i x Co un t i es most

likely f l ow ed toward

the northwest.

R E L A T I O N S H I P OF TEE B E D R O C K SU RFA CE TO T O P O G R A P H Y
N o r t h of Mancelona,
the b e d r o c k su r f ac e
Con spicuous,
lowlands,

su r f i c i a l

but di s p l a y s hi g he r rel ie f

northwest-southeast

c a ll ed

t o p o g r a p h y mi mi c s

ori en te d

"th ro ug h val ley s"

(Fig.

flat-bottomed

in this

study,

al ig ned w i t h s i m i l a r l y o r i e n t e d b e d r o c k va lleys.
addition,
Co m p l e x

7).

are
In

the n o r t h e r n m o s t tr a ct s of the In ne r Port H ur on

(named the

"apex"

co in ci de w i t h the h ig he st
study ar e a

(T.

32 N.,

Mancelona,

however,

in this di sse rta tio n;
k n ow n b e d r o c k a l t i t u d e

R. 4 W.;

l o c al iz ed

b ed ro ck and s u r fi ci al

Fig.

Fig.

6).

in the

S o u t h of

relationships

between

t o po g r a p h y are we a k or non-

4)

A

A'

1400 .

ELEVATION I
N FEET

1300 *

F Iu t
1000

-

JF.

f

*5

i

‘^VV,

BOO

fig v

.

£*'•t‘

dfiift

Ip fll
.

700'

BEDROCK
600.

WNW
0

ESE
6 mi

10 mi

Figure 7. Profile A-A,' show n on Figure 5, show ing the
"relationship of the bedrock surface to topography.

31

existent

(Fig.

8).

K a l k a s k a Valley,

the b e d r o c k su rf a c e map,

so c o n s p i c u o u s

on

is c o m p l e t e l y m a s k e d at the

surface.
Melhorn

(1954,

p.

29)

states

that:

in it ia l v a r i a t i o n s in (har dn ess a n d li tho log y)
p r o b a b l y p r o d u c e d a p r e g l a c i a l t o p o g r a p h y in w h i c h a
n o r t h w a r d - f a c i n g c u e s t a had b e e n d e v e l o p e d on the
M a r s h a l l Sa nds ton e.
This c u e s t a faced a l o w l a n d belt
to the n o r t h d e v e l o p e d on so f t e r Antrim, E l l s w o r t h and
C o l d w a t e r S h a l e s ... G l a c i a l e r o s i o n and d e p o s i t i o n
m o d i f i e d (the bed rock) p a t t e r n but did not c o m p l e t e l y
ob sc u r e it, so th at the old t o p o g r a p h i c r e l a t i o n s h i p s
are still e v i d e n c e d in l e s s e r d e g r e e on the p r e s e n t
surface.
For example, the Po r t H u r o n m o r a i n e
t h r o u g h o u t the r e g i o n c l o s e l y follow s the a p p r o x i m a t e
p o s i t i o n of the s ca rp fr o n t i n g the old M a r s h a l l
cuesta.
T h o u g h re as ona bl e,

this

interpretation

is not

s u b s t a n t i a t e d by b e d r o c k s u rf ac e data.
altitudes
Marshall

fr o m T.

26 N . , R.

Formation

In the a d j o i n i n g

6 W.,

(Milstein,

township

u n d e r l a i n b y the

1987),

(T.

Uppermost bedrock

average

27 N . , R.

230 meters.

6 W.)

altitudes

on the C o l d w a t e r S h a l e a v e r a g e

195 m and th er e

g r a d a t i o n of b e d r o c k a l t i t u d e s

a c r o s s the l i t h o l o g i c

b o u nd ar y,

r a t h e r t h a n a d i s t i n c t es ca rpment.

a p p a r e n t a b s e n c e of a M a r s h a l l
not

e a s i l y ex pl a i n e d ,

but

c u e s t a in the

indicates

is a

This
region

is

factors o t h e r th a n

local c o n f i g u r a t i o n of the b e d r o c k s u r f a c e m a y be
responsible

for p o s i t i o n i n g of the P o r t H u r o n Complex.

In addition,

M e l h o r n ’s q u o t e

i mp lie s

Po r t H u r o n fe a t u r e c l o s e l y p a r a l l e l s
subcropping
(1936),

litho lo gi es .

that the

the p a t t e r n of

M a r t i n ’s m a p of b e d r o c k g e o l o g y

w h i c h M e l h o r n cited,

shows the n o r t h e r n b o u n d a r y

B

B'
Outer

Port

DRIFT >£:

Kalkaska Valley

BEDROCK

Figure 8. Profile B-B,' show n on Figure 5, show ing the
relationship of the bedrock surface to topography.

Huron

Complex

33

of the M a r s h a l l

formation trending

southwest-northeast

a c r o s s K a l k a s k a a n d O t s e g o C o u nt ie s,
the t r e n d of the O u t e r Port H u r o n

feature.

geologic map

(Milstein,

in fo rmation,

shows a m u c h d i f f e r e n t

east-west

1987),

s o m e w h at p a r a l l e l i n g
T he

latest

b a s e d on more d e t a i l e d
boundary,

oriented

t h r o u g h K a l k a s k a an d C r a w f o r d Coun ti es ;

s o u t h w e s t e r n K a l k a s k a C o u n t y do es
the O u t e r Port H u r o n position.

only in

the trend c o i n c i d e wi t h

Certainly,

the Port H ur on

C o m p l e x b r o a d l y p a r a l l e l s the t r e n d

of the M i c h i g a n

s t r u c t u r a l basin,

two Port H u r o n

margins

extend across

Col dw at er ,
Th is

in det ai l

the

three l i t h o l o g i c u n i t s

E l l s w o r t h / A n t r i m fo r m a t i o n s ;

s u gg es ts

positioning
a lo ne

b ut

that b e d r o c k i n f l u e n c e s

are var ia bl e,

can no t

acount

and that

(Marshall,

Mils te in,

1987).

on t o p o g r a p h i c

subcropping

li t h o l o g y

for the l o c a t i o n of the P o r t H u r o n

Complex.
In short,

the ap p a r e n t a b s e n c e of the M a r s h a l l c u es t a

and p o o r r e l a t i o n s h i p b e t w e e n b e d r o c k and s u r f i c i a l
topography
we r e

not

i n di ca te

that

significant

the O u t e r Po r t H u r o n

factors

bedrock characteristics

in c o n t r o l l i n g p l a c e m e n t

trend in the s o u t h

r e g i o n a l b e d r o c k c on t r o l
C h a p t e r 3).

local

of the

N o r t h of Mancelona,

topography exerted a significant
la ndscape,

as

(arguments

for

f e atu re are p r e s e n t e d
however,

in

bedrock

in f lu en ce

on th e m o de rn

i n d i c a t e d by c o i n c i d e n c e of b o t h

surfaces,

and c o r r e s p o n d e n c e of hi g h b e d r o c k w i t h the

I n n e r Port

H u r o n apex.

exhibit

Thus,

of

the Port H u r o n C o m p l e x e s

34
strong c o n t r a s t i n g

relationships between bedrock

t o p o g r a p h y and m o d e r n t e r r a i n
pa rts

in n o r t h e r n v e r s u s

so u t h e r n

of the st ud y area.

RELATIONSHIP BETWEEN
THROUGH VALLEYS AND BEDROCK VALLEYS

Bedrock valleys

a p p a r e n t l y have

of m o d e r n t h r o u g h valleys,
dr if t

thickness exceeds

even

in areas w h e r e

100 meters.

landscapes which reflect details
Pleistocene paleo-surface
by R i e c k and W i n t e r s
relationships

process

valleys

of an older,

creates

"palimpsest"

They attribute

the a b l a t i o n of
(Fig.

9).

su c h

ice in p r e ­

a l o w l a n d o v e r l y i n g the old b e d r o c k
result

s t a c k e d one on top of the other,

the t r e n d of the o r i g i n a l valley.
also e x p l a i n c o i n c i d e n t v a l l e y s
If so,

the p r e s e n c e

in g l a c i a t e d

in a ser ie s of
each reflecting

Suc h a p r o c e s s may

in t h i c k d r i f t
of p a l i m p s e s t

in C h a r l e v o i x and A n t r i m C o u n t i e s e x p a n d s
of this c o n c e p t

the

E v e n t u a l l y this

R e p e a t e d g l a c i a t i o n s may

s tu dy area.

buried

in s o u t h e a s t e r n M i c h i g a n to first

stream valleys

channel.

average

Modern glaciated

have b e e n c a l l e d

(1979).

a c c u m u l a t i o n and l a t e r
ex i s t i n g

influenced placement

in the
topography

the a p p l i c a t i o n

regions.

CONCLUSIONS
T r e n d of the
(Fig.

Inner and O u t e r Port H u r o n C o m p l e x e s

5) a p p e a r s to be u n r e l a t e d to s u b c r o p p i n g

lithology,

as m a p p e d by M i l s t e i n

(1987).

b e d r o c k t o p o g r a p h y p r o b a b l y do e s c o nt ro l

bedrock

Ho wever,
the l o c a t i o n of

35

BEFORE GLACIATION:
STREAM VALLEY CUT INTO DRIFT
AND/OR

BEDROCK

a

ADVANCING ICE FLOWS INTO AREA.
FILLING VALLEY

\
/ /

AS GLACIER MELTS. ICE LINGERS
IN MORE PROTECTED VALLEYS AND IS
COVERED BY OUTWASH SEDIMENTS

WHEN ICE FINALLY MELTS,
A SERIES OF DEPRESSIONS IS LEFT.
DELIMITING THE FORMER VALLEY COURSE
D R IF T

Figure 9. Proposed gen esis of coincident valleys(from Blewett, 1984).

36

the Inner Po rt H u r on apex,
in e a s t e rn Charlev oix ,
A n t r i m Co unties.

and

w e s t e r n Otsego,

In addition,

Ch a p t e r 3 d o c u m e n t s a strong
low lands a n d re gio na l
Ou ter Po r t H u r o n

influences

the t o p o g r a p h y

and n o r t h e r n

eviden ce p r e s e n t e d

in

r e l a t i o n s h i p b e t w e e n be dro ck

la n d f o r m pa tterns

of the Inner and

features.

S E D I M E NT S A S S O C I A T E D WITH THE
I N N E R AND O U T E R PORT H U RO N CO M PL EX ES

A p p l i c a t i o n of the m o r p h o s e q u e n c e
req uires

1 ) i d e n t i f i c a t i o n of

co nc ep t here

facies ch a n g e s

for the

Inner Port H u r o n and O u t e r Port H u r o n features,
ev idence that
sediments,
dep os it s

ic e-c ontact

and pr og la ci al

r a t h e r than till,

surf ic ia l

in areas p r e v i o u s l y map pe d as m o r a i n e

and Taylor,

1915;

ma p p i n g and

se dim en t a n a l y s is were n e c e s s a r y

part of the

investigation.

Aspects

of P l e i s t o c e n e

th i ck ne ss w e r e

1982).

(Leverett

B o t h de tailed
for this

s t r a t i g r a p h y and drift

a n a l y z e d from w a t e r and p e t r o l e u m well

logs on file at the G e o l o g i c a l

Survey D i v i s i o n of the

M i c h i g a n D e p a r t m e n t of Na t u r al

Resources.

sediment d a t a we r e d er i v e d
stone piles,

2)

glaciofluvial

are the m a j o r

F ar ra nd and Bell,

plus

roadcuts,

Surficial

from gravel pits,

soil maps,

and other exposures.

D rift th ickness
A drift

th i c kn es s map

a p p r o x i m a t e l y 400 well

for the area,

b a s e d on

log d a t a points and s u p p l e m e n t e d

37

wi t h data from R.L.
permission),

R ie ck

is s h o w n

(1981,

in Fig ur e

1985;
10.

us ed wi t h

C o n t o u rs are drawn

in feet to m a t c h the well log d a t a and the v a l u e s
p r o v id ed by R.L.
(170 m),

Rieck.

and the m a x i m u m

Average
(953

ft,

th ickness
290 m)

d e ep es t v a l l e y on the b e d r o c k surface.

is 550

feet

is ov e r the

Thickness

contours

tr en d p e r p e n d i c u l a r to the Inner and O u te r Port H u r o n
margins,

and v a l u e s

te n d to

reaching a m a x i m u m of 843
at the

increase n o r th ea st wa rd ,

ft

(257 m)

Inner Po r t H u r o n apex.

misleading,

however,

thi ck ne ss v a l u e s
valu es become

in T.

T he se

trends

b e ca us e a l t h o u g h

g r e a t e r tow ar d the
is ob sc u r e d

n u m b e r of d a t a p o i n t s

R.

4 W.

somewhat

in dividual

south

(Figs.

in Figure

average
7 and 8).

10 b e c a u s e

the

is i n s u f f i c i e n t to show g r ea t e r

drift th i c k n e s s v a r i a b i l i t y

in no r t h e r n areas.

As re ve a l e d by a c o m p a r i s o n of Figures
in g l a c i a l depos it

w i t h l o c at io ns of p r o m i n e n t

3 and

10,

th i c k n e s s do not c o r r e s p o n d

to p o g r a p h i c

suggests that d r i f t t h i ck ne ss

alone

e x p l a i n tre nd s of m a j o r t o p o g r a p h i c
area,

are

are h i gh es t t o w a r d the north,

This r e l a t i o n s h i p

va ri a t i o n s

32 N.,

features.

is i n a d e q u a t e
elemen ts

This
to

in the study

with the p o s s i b l e e x c e p t i o n of the Inner Port Hur on

apex.

bedrock

R e l a t i o n of d r i f t .
f o r m . and m o d e r n t o p o g r a p h y

The s t u d y ar e a c an be s u b d i v i d e d

into n o r t h e r n and

sou th er n s e c t i o n s b a s e d on d r i f t / b e d r o c k relationships.

IN N E R
h

I)

500 450
(/ [no

c -Jl

U r o \\ ^

V- A I N

^

^ANC

E^-°

J%\-°P£

8a

CONTOUR INTERVAL:50FEET

Figure 10. Drift th ick n ess in the Inner and Outer
Port Huron C om plexes

39

S o u t h of M a n c e l o n a gl aci al

sediments

ob sc ur e

su r f a c e c h a r a c t e r i s t i c s and r e l a t e d v a l l e y s
i d e n t i f i e d o n l y as li ne a r a re as
map.

In cont ra st ,

show st ro ng

sediments

bedrock

in the

of th ic k d e p o s i t s on the

b e d r o c k t o p o g r a p h y and d r i f t

s u b su rf ac e

Th ic k

(Fig.

7);

th in d e p o s i t s

high

cover

b e d r o c k valleys.

b e t w e e n n o r t h e r n and

is d e e p l y buried,

in the

form of kett le chains

R eg i o n a l

to ma r k a t r a n s i t i o n

s ou th er n sections.

valley

A l t h o u g h this

it is e x p r e s s e d at the

differences

de po si ts ,

in d r i f t / b e d r o c k

irregularities

which,

once exceeded,

in b e d r o c k top og rap hy.

topographic

in the

relationships
t h r e s h o l d of

works
Meek

to ma s k

(1984)

e x p r e s s i o n of the b e d r o c k s u r f a c e

f u n c t i o n of b e d r o c k relief and d r if t
expressed

surface

and dry channels.

m a y be r e l a t e d to a p a r t i c u l a r t h i c k n e s s

that

th i c k n e s s

at the Inner Port H u r o n ape x mi mic

The A l b a b e d r o c k va l le y a p p e a r s

gl aci al

are

c o r r e s p o n d e n c e n o r t h of Ma nce lon a.

gl ac ia l

adjacent

bedrock

thickness

found
is a

as

form:

+ 10 meters

w h e r e T = a v e r a g e dr if t
bedrock relief

in meters.

of the eq ua ti on ,
l i k e l y will
be r e f l e c t e d
Data

t h i c kn es s

in me te r s

When T exceeds

and R b = m a x i m u m
the

right

th en the form of the u n d e r l y i n g

be masked.

If T is less,

bedrock

side

surface

form will

in p r e s e n t to po graphy.

fr o m the

s tud y are a

substantiate

a p p l i c a t i o n of

40
these

fi nd i n g s

in part:

N o r t h of M a n c e l o n a
T = 6 4 m

R b = 1 8 3 m

64 <

The

101.5 m

form of the b e d r o c k s u r f a c e wi l l be ev i d e n t

in the

topography.

South of M a n c e l o n a
T = 156 m

Rb = 131.1

156 m

>75.6

m

m

The form of the b e d r o c k s u rf a c e will

be m a s k e d

at the

surface.
Though

th es e e q u a t i o n s w e r e

areas w i t h t h i n n e r dr if t
re a s o n a b l e

accounting

developed

for b e d r o c k / d r i f t

Subsurface

relationships

feature.

logs p r o v i d e

li mi te d i n t e r p r e t a t i o n s of s u b s u r f a c e
Inner and O u t e r Po r t H u r o n Co mp l e x e s .

Rugg Pond

a

stratigraphy

W a t e r and p e t r o l e u m we l l

for some of t he se

lo c a l i z e d

(15-35 m ) , th e y do p r e s e n t

ob s e r v e d on the I n n e r Port H u r o n

along the d e e p l y

for

the b as es

stratigraphy

for

in the

A few o u tc ro ps

incised Rapid River provide verification
interpretations,

and an e x p o s u r e

reveals a Pleistocene paleosurface

near

recognized

on the ba si s of g l a c i a l l y b u r i e d w o o d and o t h e r o r ga ni c
matter

that has b e e n

(U
C dated.

All

are d i s c u s s e d below.

41
S UB SU R F A C E SE DIMENTS A S S O C I A T E D WI TH THE
INNER PORT H U R O N C O M P L E X
F ig ur es
about

11 and

200 well

up p e r m o s t

logs,

12, wh ic h are based on data
show,

respect ive ly,

sand and gravel deposits,

underlying

(45 m)

in pro ximal

Inner Port H u r o n crest)
distally

170

ft

and v a r i a t i o n s

270

ft

regions

is from

(areas cl o s e s t

from the crest).

in the

A v er ag e

sand and gravel unit

to less th a n 40 ft

(areas farthest

va l u e s exce ed
and

the t h i ck ne ss of

clay surface wi th i n the study area.

t h i c k ne ss of the u pp erm ost
150 ft

from

to the

(10 m)
Maximum

(80 m) at the Inner Port H u r o n apex

(50 m) n o r thw est of Mancelona.

The K a l k a s k a

and D a r r a g h b e d r o c k valleys also d i s p l a y thick
sediments.
surface,

A small,

ch ap te r

high-altitude terrace

3) has thicke r de p o s i t s

(Camp Te n

along

its

n o r t h w e s t margin.
Vol u m e of the uppe rm ost

sand un i t

in the

s tu dy area

is a p p r o x i m a t e l y 6 km3 based on the e x p r e s s i o n
V = l / 2 (l * w * h ), wh er e V=volume,
w = w i d t h of the sandur.

l = l e n g t h of the s a n d u r ,

arid h = t h i c k n e s s of d e p o s i t s at the

Inner Port H u r o n crest.
Fig ur e
and shows

13 uses co mb in ed d a t a

is inclined no rth westward.

discussed

11 and

12,

that u p p e r sand and g r a v e l s were d e p o s i t e d upon

clay w i t h a surfa ce of m o d e r a t e
that

from Figur es

re li e f

(165

ft,

I m p l i c a ti on s

50 m)

of this are

in C h a p t e r 4.

C ol le cti ve ly,

four lines of ev i d e n c e

u n d e r l y i n g cl a y is till:

s u gge st that the

100

150

20C>

250

150

1

150
100

s— 100

100'

100
100

50~vX
MANCELONA

| ou
PLAIN

ioo

-^— ioo—
100

CONTOUR INTERVAL:60FEET

Figure 11. T h ick n ess of the upperm ost sa n d and gravel unit.

f

I

1050J

_ s

>— 1100

w ^ncelona

L

2

CONTOUR INTERVAL:50FEET

Figure 12. Altitude of the underlying clay surface.

NW

SE

ELEVATION I
N FEET

OUTER PORT
HURON COMPLEX

1200--

INNER PORT HURON COMPLEX

CLAYSURFACE

0

1 mi

2 rri

3mi

4 rri

Figure 13. Relation b etw een m odern topography and the underlying
clay surface. Profile location show n in Figure 5.

45

1) b r o w n till
R iv er V a l l e y

is e x p o s e d along the wes t
(SE1/4,

SW1/4,

T.

28 N.,

side

R.

of the Rapid

7 W. ) at an

e l e v a t i o n of a p p r o x i m a t e l y 282 ra, well w i t h i n th e
of a l t i t u d e s
m;

F i g . 1 2).

2)

sa mpl es

rev ea l

for the highes t

fr o m two

that till

3)

lineated

4)

Fig.

12) and m a y r e p r e s e n t
pr es en t

pre-existing

(Fig.

12).

Th is

cla ys

are

ice-marginal

of

till

upon a

surface.

lacustrine.

lacustrine deposits

such e x t e n s i v e

p r o b a b l y for me d

in an ic e - f r e e

env iro nm en t,

are u s u a l l y flat,

if

or

r a t h e r th a n s u b g l a c i a l l y .
of l a c u s t r i n e dep osi ts

any v a l l e y e x i s t i n g on this

cut b y su bs eq ue nt

a ft er d r a i n i n g

is r e q u i r e d

First,

b e c a u s e u n a l t e r e d s u rf ac es

m e l t i n g of

in the

is a c c o m m o d a t e d

A mor e c o m p l i c a t e d mode of d e p o s i t i o n

mu st be a)

b u ri ed

on the cl a y surface c o r r e s p o n d w i t h axes

si mp l y b y u n i f o r m d e p o s i t i o n of basal

Second,

(based on

in n o r t h w e s t e r n A n t r i m County.

major bedrock valleys

these

in the

clay su r f a c e s ap pe a r to be

of s t r e a m l i n e d l a n df or ms

la n d s c a p e

valleys

mo s t

r ep or te d

et a l ., 1986).

underlying

c o n t o u r pa tt ern s;

modern

to th ose

in a n o r t h w e s t - s o u t h e a s t d i r e c t i o n

equivalents

- 290

gas we ll s on the M a n c e l o n a P l a i n

co mp a r a b l e

(Wi nters

In places,

(275

is b e n e a t h the u p p e r m o s t san d and gravel

unit at a l t i t u d e s
st udy area

cl a y s u rfa ce h e r e

range

of the lake,

ice b l o c k s b u ri ed

su rfa ce

s t re am e r o s i o n d u r i n g
or b)

or

f o r m s u b a e r i a l l y by

in p r e - e x i s t i n g

l o w l a n ds

46
prior

to lake

formation.

Once

formed,

t he n be b u r i e d by sand and gravel.
mod el

v a l l e y must

T h o u g h possible,

seems o v e r l y c o m p l i c a t e d c o m p a r e d

d e p o s i t i o n of

this

this

to simp le

till.

S U B S U R F A C E S E D I M E N T S A S S O C I A T E D W I T H THE
O U T E R PORT H U R O N C O M P L E X
Subsurface

clay deposits

O u t e r Port H u r o n Complex,

making

in the O u t e r Port H u r o n ap e x
significant underlying
clays

relatively

s e d i me nt s

discussed

that

these

An exposure
su p p o r t s

S o u t h of the apex,
complicated.
proximal
Elmira,
w el ls
la ye rs

Only

4 W . ) is any

identified.

Here,

b e n e a t h the c re st of the

(4-7 m)

and

2)

Their

cl os e

s t a g n a t i o n t o p o g r a p h y and s t r a t i f i e d

su gg e s t

below,

31 N . , R.

and are abs en t di stally.

shallow depth

a b l a t i o n till.

in the

a n a l y s i s diffic ul t.

clay p a t t e r n

feature

association with

c la ys may be

flow or

of till at F l e m i n g ’s farm,

this

i n te rp ret ati on.

d i s t r i b u t i o n s are e v e n more

Logs r a r e l y r e c o r d cla y b e n e a t h the

t r a c t s of the O u t e r Port H u r o n C o m p l e x east of
where

some w e l l s

east of A l b a do,

are

93 m deep.

however,

s e p a r a t e d by sand a n d/ o r

has also b e e n
the O u t e r

l o gg ed at d e p t h s

Port H u r o n

p a t t e r n here
the

(T.

are c o n c e n t r a t e d at d e p t h

O u t e r Port H u r o n
1)

are h i g h l y v a r i a b l e

fe atu re

may be r e la t e d

ice m a r g i n

in this are a

Mos t

logs

report n u m e r o u s
sand and gravel.

from

clay
Clay

of 50-60 m in re gio ns

south of A l b a airport.

of
The

to s u c c e s s i v e p o s i t i o n s of
(Lakes of the N o r t h margin;

47
Ch.

3).

East of

M a n c e l o n a the

surfa ce v a r i e s

from 15-70

m in depth,

wi t h

a mode of a p p r o x i m a t e l y

35-40 m.South

of C r a w f o r d

Lake

clays are w i d e s p r e a d

the

and te nd to be less deep ly

in

su bs u r f a c e

buried.

Co m b i n e d w i t h alti tu de s of the m o de r n

surface,

e l e v a t i o n s of the sub cr op pi ng cl a y surfac e d e fi ne
thi ck ne ss

of the up pe rmo st

sand and gravel

c o m p r i s i n g the O u t e r Port H u r o n Complex.
cl ay d i s t r i b u t i o n s
but,

in general,

d ep osi t
w ed ge

thi cke st

here makes

unit
V a r i a b i l i t y of

i n t e r p r e t a t i o n difficult,

this high er unit
in pro ximal

the

forms a w e d g e - s h a p e d

regions.

Farther

sou th this

is less well defined.

RUGG POND SITE
G l a c i a l l y b u r i e d organic d e p o s i t s
above the base of the bluff
Po nd D am

(SE1/4,

NW1/4,

5 m

i m m e d i at el y n o r t h of Rugg

NE1/4,

n o r t h e r n K a l k a s k a County.

are e x p o s e d

sec.

31,

T.28N.,

F l a t t e n e d wo o d

R.7W.)

fragments

and

ot her c a r b o n a c e o u s m a t er ia ls are w i t h i n a silt

lying

be tw e e n two

The wood

yi e l d e d a

br ow n tills

,4C date of

(10 YR Y/2,

Fig.

>41,000 y r s . B.P.

i4).

in

(Beta - 29495 );

p r e l i m i n a r y a n a l y s i s of a r e lat ed p o l l e n a s s e m b l a g e
(Marlette,

u n p u b l i s h e d material,

1989)

ac c u m u l a t i o n u n d e r n o r t h e r n boreal
conditions.

Layers

45 de gr ee s tow ard
edge,

in di c at i ng

co ntai ni ng

indicates

or s u b a r ct ic

c a r b o n a c e o u s m a t e r i a l dip

the north at the e x p o s u r e ’s n o r t h e r n
that the d e po si ts

have b e e n deformed.

The s t r a t i g r a p h y a s s o c i a t e d w i t h the Rugg

Po n d

site

is shown

in Figure

14.

cons is t s of l a c us t ri ne
are 1) thin,
deposits,

Ne ar l y two thirds
fine sand and silt.

Till

lenses

2) u s u a l l y se p a r a t e d by sand and silt

and 3) c o n f i n e d to the lower p a r t s of the

exposure.

Till

1 lies highest

in the c o l u m n and

a s s o c i a t e d w i t h the or ganic material.
above

of the outcr op

the o r g a n i c - b e a r i n g

silts,

Till

and till

is not

2 is di re c t ly

3 lies

underneath.
A l t h o u g h s t r a t ig ra p h ic da ta are
the small

size of the outcrop,

till

li mit ed b e c a u s e of
2 m a y m a r k a pr e-Late

Wisconsinan

ice ad van ce becau se

than 41, 00 0

years old as so c i a t e d w i t h "cold"

Age and d e p o s i t i o n a l
color and t e xt ur a l

it buries w o o d gr eat er

h i s t o r y of tills

si m il ari tie s

to till)
finding

ice m a r g i n a l d e p o s i t s

( + 100 m)

et a l . (1986).

apparently consisting

(as oppos ed
a

for thick

in the area as r e p o r t e d by

Figure

14 shows that on l y about
is till,

of l ac us tr in e

w i t h the rest

silt and o t h e r

ice

deposits.

C o m p a r i s o n w i t h n e a r b y or ga ni cs
deposits

d e m o n s t r a te

in a g r e e m e n t w i t h d e t a i l e d s t r a t i g r a p h y

25% of the s t r a t i g r a p h i c c o l u m n

ma rg i n a l

In

in this part of the Inner Port H u r o n Complex,

sec ti on s of drift
Wi n t e r s

3 and 2

same deposi t.

this o ut c r o p and r e la te d se d i m e n t s

the g r e a t a b u n d a n ce of

3 are unkno wn

be tw ee n tills

suggest that th ey may be part of the
addition,

1 and

pollen.

are r e p o r t e d

of K a l k a s k a

-- Y o u n g e r o r g a n i c

from four c l o s e l y s p a c e d w e l l s west

(Winters et a l ., 1986),

at a l t i t u d e s

75 m

49

A
B

8.5 m

»

4

»4
*«

w* *

4

*^

4 ►«

A-

GLACIOFLUVIAL (?) SAND AND GRAVEL, UNDIFFERENTIATED;
NON-CALCAREOUS

B-

ALTERNATING LAYERS OF LACUSTRINE SILT AND CLAY;
CALCAREOUS

C-

LACUSTRINE FINE SAND AND SILT WITH CLAY LENSES; LOOSE,
POWDERY, SLIGHTLY TO NON-CALCAREOUS

D-

DENSE LACUSTRINE SILT WITH OCCASSIONAL CLAY STRINGERS;
CALCAREOUS

E-

TILL #1. BROWN GRADING TO GRAY; CALCAREOUS

F-

GLACIOFLUVIAL (?) SAND, UNDIFFERENTIATED; NON-CALCAREOUS

G-

TILL #2. BROWN, CALCAREOUS

H-

LACUSTRINE SILT CONTAINING ORGANIC MATERIAL; CALCAREOUS

I-

TILL #3. BROWN, CALCAREOUS, WITH SAND INCLUSIONS

J -

GLACIOFLUVIAL (?) SAND, UNDIFFERENTIATED, WITH TILL
INCLUSIONS; CALCAREOUS

G
H
|
J

SLUMP
TILL 2

SLUMP
WOOD > 41,000 yrs

'J.

VLL3

SLUMP

Figure 1 4 . Rugg Pond Stratigraphy.

50

lo w e r

th an the Rugg Pond site.

botanical

data

in di c a t e that a bo ut

was

ice-free,

and

later a c l o s e d b o r e a l

organic

R a d i o c a r b o n d a t e s and

p o o r l y drained,

and s u p p o r t e d

forest.

h o r i z o n is at or near

or g a n i c

its o r i g i n a l

significantly,

in situ at

or hi gh e r
at

Thus,

at 35,0 00

these two

another.

the same

yrs.

B.P.

altitudes

Curiou sl y,

is fu rt he r e v id en ce

t o p o g r a p h y her e

75 m.

then

This

of bu r i e d

yrs. old are

site had to be as high

l o c a t i o n s are w i t h i n

Th is

alti tu de ,

at least

if o rg an ic s >4 1 , 0 0 0

255 m,

first an open

if not t r a n s p o r t e d

record approximate

paleosurfaces.
found

deposits,

the area

If the Ru g g Po n d

M i d d l e W i s c o n s i n a n p a l e o r e l i e f was
is so b ec au s e

35,000 B.P.

is not palimpsest,

modern

10 m a l t i t u d e

surfaces
of one

that pr es e n t
and that La t e

W i s c o n s i n a n g l a c i a t i o n has bo th t r a n s f o r m e d the
t o p o g r a p h y and

s u b d u e d the relief.

S u r fi ci al
Surficial

sediment

in the

predominantly glaciofluvial
almost wholly

s t u d y ar e a is

sand a nd gravel;

till

is

r e s t r i c t e d to f l u t e d u p l a n d s a n d the Post

I n n e r Port H u r o n
common

s e d i m en ts

in a r e a s

zone

(Fig.

15).

immediately up-ice

O u t e r Port H u r o n

fe at ur es

and

proximal outwash

facies.

Details

Lacustrine deposits
from the

are

I nn er and

in a s s o c i a t i o n w i t h
of each are d e s c r i b e d

below.
Sedimentological

i n v e s t i g a t i o n of nine g r a v e l

pits on

51
the M a n c e l o n a P l a i n ’s most e x t e n s i v e
surface;
study.

Ch.

3)

taken v e r t i c a l l y at ea c h pi t and

into c o a r s e

fractions.

(>8

Li tho lo g y,

mm)

fragments.

calculated
phi

mm)

a n d fine

r o un dn ess

va lu e s we r e d e t e r m i n e d
( >8

(Elmira

c o n s t i t u t e d a m a j o r p o r t i o n of this

S am p l e s w e r e

separated

surface

(< 8 mm)

and p r i n c i p a l

for 75 r a n d o m l y

axes

s e l e c t e d coa rs e

Sp he ri c i t y and fla tn es s wer e

fr om axis

data;

in te rva ls of one

unit.

fine

f r a ct io ns w e r e

s i e v e d at

B e d f o r m l i tho fa cie s,

p a l e o d i s c h a r g e s , and paleocurrent directions

als o were

determined.
Discarded

sto ne s

are pi le d

al ong

ro ads

lo c a l i z e d

facies w e r e

re co ver ed du ri n g
north of Alba.

a x e s wer e d e t e r m i n e d

s a m p l e d sto ne s

wer e m a p p e d
boulders

cm)
(Fig.

i 1 m.

facies ch an g e s
successive

Lithology,

of

five

such

roundness,

for 50 r a n d o m l y -

from each pile.

Pl ac es w h e r e
d i a m e t e r >50

area.

harvesting

Some a s p e c t s

i n t e r p r e te d by sam pl in g

stone pil es w i t h i n a 15 mi.
and p r i nc ip al

pot at o

th re e or more
exist within
15),

s u r f ic ia l

( b-

100 - 150 m of one a n o t h e r

as were

l o c a ti on s

T h e s e data we re use fu l
in surfi cia l

boulders

sediments,

of

sin gl e

in 1)

recognizing

and 2)

determining

ice m a r g i n a l positions.

S U R F I C I A L SE DI ME NT S O F THE
I N N E R PORT H U R O N C O M P L E X
The o v e r a l l
se di me nt
su rfa ce

sizes

sta ti st ic al

d i s t r i b u t i o n of

fro m nine grav el pits

is s h o w n

in Fig

16.

on the

Finer t e xt ur es

Elmira
co ns i s t

52

-11 -10

-9

-8

-7

-6

-5

-4

-3 -3

-2

-1

0

1

2

3

4

SIZE (phi m easure)

Figure 16. Overall distribution of c o a rse and fine sed im ents.

53
p r e d o m i n a n t l y of m e d i u m and coarse
d i a m e t e r of the co ar s e

sands.

M e a n b-axis

fraction is 2.8 cm,

with

a

v a r i a n c e and s t a n d a r d d e v i a t i o n of 3.8 and 1.9 cm,
res pectively.

K u r t o si s

r e l a t i v e l y high

(13.2;

for the overa ll

in the population.

positively

indica ti ng

clasts

in pr oxi ma l

locations.

clasts

in the o ve ra ll p o p u l a t i o n are
sedimentary,

Roundness,
Fig ur e

17.

wh er e a s

flatness,

G re a t e r

flatness

the shape

sorted m i d - s a n d u r

The d i s t r i b u t i o n

skewed,

non-carbonate

is

the p r e s e n c e of a few large

and

L i t h o l o g i c a l l v , coa rs e
60% carbonate,

and s p h e r i c i t y are

and s ph eri ci ty are

terms

Most large cla st s

sh ow n in
abrasion,

that des cr ib e

in this

ro und ed to su b- r o u n d e d and r e l a t i v e l y compact,
sand ur c h a r a c t e r i s t i c s

re po rte d e l s e w h e r e

C o m p a r i s o n of sed im en t c h ar ac t e r i s t i c s
Me a n b- ax i s va l u e s are gr ea tes t
pits

(Crego and C - K pits;

most dist al
variance

site

(DNR pit;

Fig.

18)

study are
typical

(Church,

1972).

among gra ve l pits

in pr ox i m al

gravel

and sm al le st

at the

18).

of

Analysis

of

(A N O V A ) in dicates that c o l l e c t i v e l y the nine

distributions
confidence

are s t a t i s t i c a l l y d i f f e r e n t

levels.

the most pr ox i m a l
it was

Fig.

25%

15% crystalline.

ro undness re fl ect s more

of a rock.

is

hi g h l y l e p t o k u r t i c ), p r o b a b l y

due to an ab u n d a n c e of e s pe c i a l l y well
samples

population

Because

at 99%

the Cr eg o and D N R sites ma r k

and distal gravel

pits,

respectively,

r e a s o n e d that their sedime nt d i s t r i b u t i o n s

not be the same.

should

The t-test was then a p p l i e d and the two

54

ROUNDNESS

VA

AN

SA

SR

RN

WR

.2 H

FLATNESS

A
0

2

A

.6

.8

H

i

.6

.8

1.0

.4 -

J-

.1

SPHERICITY

-

0

i

I
.2

r

.4

1.0

Figure 17. R oundness, flatness, and sphericity of
coarse clasts from gravel pits on the Elmira surface.

55

4.1
CREGO

3.8
ELMIRA
3.0

2.9
ASPHALT
ALBA

2.5

NEW WILKES
LOWER
WILKES UPPER WILKES 2.4
2.3

DNR
1.9

Figure 18. Mean B-axis diam eter of c o arse clasts from
gravel pits on the Elmira surface.

56

sites wer e

fo und to be s t a t i s t i c a l l y di f f e r e n t

at 99%

c o n f i d e n c e values.
Sphericity

(Fig.

n a r r o w clasts)
Visu al ly ,
distal

to one

portions

can range

B- ax i s

a,b,

(long,

a n d c axes).

a p p e a r to be a s s o c i a t e d wi t h the

of the sandur,

that d i f f e r e n c e s

statistically

from ne a r ze r o

(clasts w i t h equal

higher values

in d i c a t e s

and,

19)

but an al y s i s

of va ri a n c e

in v a r i a b i l i t y are no t

signi fi ca nt .

variance

in theory,

(Fig.

20)

populations

measures

near

e x p e c t e d to y i e l d h i g h e r va lu e s
s o r t e d co n d i t i on s.

This

the

relative

sorting

ice m a r g i n w o u l d be

representing poorly

is s u b s t a n t i a t e d by d a t a from

the E l m i r a surface.
Theoretically,
di stally,

due

grav el

recorded across

the

"very a n g u l a r"

(Fig.

21).

rounded

to g r e a t e r a b r a s i o n from l o ng er

No d i s c e r n i b l e v i s u a l

as

s h o u l d be c o m e more

Thus,

difference

sandur,

in gravel

transport.

r o u n d n e s s was

e x c e p t that rocks c l a s s i f i e d

w e r e r e s t r i c t e d to 4 p r o x i m a l

pits

e xc e p t

deposited

at the g l a c i a l margi n,
s a n d u r have u n d e r g o n e

for a small p e r c e n t a g e

n e a r l y all large

cl as t s

c o n s i d e r a b l e abrasion,

on the

a l t h o u g h the

a mo u n t d i r e c t l y r e l a t e d to t r a n s p o r t on the E l m i r a sandur
al one

cann ot

be d et er mi ne d.

Characteristics
F ig u r e

22.

coarse/medium
proximal

of finer

Proximal

s h o w n in

gravel pi t s c o n t a i n a h i g h e r

sand ratio

and d i s t a l

se di me nt s are

tha n dis ta l pits.

Selected

d i s t r i b u t i o n s are s t a t i s t i c a l l y

57

0.737,

0.710

0.730
0.732
0.720

0.744

0.746

Figure 19. M ean sphericity of co a rse cla sts from gravel
pits on the Elmira surface.

r

58

^
3.9

8.2

2.1
2.7
0.9

1.2

0.6

Figure 20. B-axis variance of c o arse clasts from gravel
pits on the Elmira surface.

59

2.8

1.2

2.6
1.1

Figure 21. Distribution of "very angular" c o arse
clasts from gravel pits on th e Elmira surface.

i

60

CREGO

SIZE(phimeasure)
ELMIRA

ASPHALT

ALBA

□

SIZE(phimeasurje)

\

SIZE(phimeasure)

SIZE(phimeasure)

WILKES

SIZE(phimeasure)
SIZE(phimeasure)

UPPER
WILKES

SIZE(phimeasure)

/
LOWER
WILKES

SIZE(phimeasure)

SIZE(phimeasure)

Figure 22. Distribution of coarse and fine sed im en ts from
gravel pits on the Elmira surface.

61
different
Wallis

at

99% c o n f i d e n c e values,

analysis

In short,
c o ar se and

of variance.
on the basis of gra ve l pit data,

fine

fractions exhibit

significant variation
higher variability
angular,

and

both

a statistically

in facies.

Proximal

locations

in te xtu re and c o n t a i n larger,

less co m p a ct

better sorted

b a se d on the Kruskal-

rocks,

whereas

and c o n t a i n smaller,

di st a l

rounder,

show

more

sites are

m o r e compa ct

sediments.

Stonepiles

—

cobble-sized
localized
Alba.

stonepiles

c l a s t s were

fa c i e s

c h an ge s

containing pebble

s a mp l e d

in o r d e r to

(Fig.

located only

23).

locations.

for m o r e c o m p a c t cl as t s

this p a t t e r n

is not

findings

support

distally

fining

to be

n o r t h of

fi n i n g

A n g u l a r and s u b a n g u l a r

in p r o x i m a l

and

inv es ti ga te

on the E l m i r a s u r f a c e

A s t a t i s t i c a l l y s i g n i f i c a n t di st a l

identified

exists

Five

c l as ts are

A weak tendency
found d i s ta ll y,

s t a t i s t i c a l l y si gn ifi can t.

gra ve l pit d a t a and s u gge st
fac ie s ch an g e ex i st s

is

but

These

that a

on the E l m i r a

surface.

Bedforms

—

B e d f o r m a n a l y s i s was u s e d

fac i e s c h a n g e s

in g l a c i o f l u v i a l

has be e n d e s c r i b e d
consists

of

in detail

i d e n t i f ic at io n,

for v e r i f y i n g

material.

(Miall,

1978;

de scr ipt ion ,

i n t e r p r e t a t i o n of suites of d i a g n o s t i c
(Miall,

1978).

Principal

u ni ts

The

te ch niq ue

1983)

and

and

l i t h o f a c i e s units

recognized

in this

study

62

9.8

12.3
8.6

A rea of
san d u r
show n

aq
6.8

Figure 23. Mean B-axis diameter (cm) of stone piles
on the Elmira surface.

63

are

shown in T a b l e
Miall

(1983)

1.
presented three outwash

r e p r e s e n t i n g prox im al ,
as sem bla ges .

Though

architectural

element

model

medial,

analysis

mod els

simple

ex p o s u r e s

in this

to use,

for co mp ari son ,

and

3)

th an a r c h i t e c t u r a l

pr in ci pa l m o d e l s

(Miall,

2)

models

lithofacies

s u p e r s e d e d by a new m e t h o d

a p p r o a c h was u t i l i z e d

is r e l a t i v e l y

and dis ta l

fac ie s

1985),

call ed

the

stu dy b e c a u s e

facies
it 1)

provides well-established

r e q u ir es
element

less

extensive

analysis.

The

include:

1) Sco tt type - P r o x i m a l
m u l t i s t o r e y gravel u n i t s
of l o n g i t u d i n a l bars.

l i t h o f a c i e s d o m i n a t e d by
d e p o s i t e d by a g g r a d a t i o n

2) D o n j e k type - Me d ia l li th o f a c i e s c o n t a i n i n g
bo th bar gr av el s and sands and p e b b l y sands;
so m e t i m e s s t ro ng ly cyclic.
3) P l a t t e type - Di s ta l l i t h o f a c i e s c h a r a c t e r i z e d
by l ow re li e f bars and cha nnels.
M a i n sed iment
types are massive, l a m i n a t e d and r i pp le c r o s s ­
l a m i n a t e d sandy silts.
A n a l t er na te
(Miall,
sands)
f la s h

d i st al

1981)

facies type n a m e d " B ij ou Cree k"

is d o m i n a t e d by 1 ith of ac ie s Sh

and r e p r e s e n t s b r ai d e d

(planar

s t r e a m s c h a r a c t e r i z e d by

floods.

S e d im en ts

fr om ea c h grave l pit on the E l m i r a

surface

we re c a r e f u l l y d o c u m e n t e d in the

field and pho to gr ap he d.

Representative vertical profiles

(Fig.

constructed

for ea c h site as a m e a n s

pre se nt at io n.

Size of ou t c r o p s

A l b a grav el p it was
Once

identified,

not

for g r a p h i c

v a r i e d widely,

i n c l u d e d due

li th o f a c i e s

24) we r e

an d the

to p o o r exposure.

a s s e m b l a g e s we r e

64

Ta bl e
Fncloc
C ode

1.
L i t h o f a c i e s and s e d i m e n t a r y s t r u c t u r e s
f lu vi a l d e p o s i t s (from Miall, 1978).

U th o fa c io s

S cdlm onlnry s tru c tu re s

Interpretation

Gms

m a ssiv e , m atrix
su p p o rte d gravel

none

debris flow
d ep o sits

Gm

m a ssiv e or
crudely b e d d e d
gravel

horizontal bedding,
imbrication

longitudinal b ars,
lag d eposits,
siev e deposits

• gravel, stratified

trough cro ssb e d s

m inor channel fills

Gp

gravel, stratified

plan ar cro ssb e d s

linguoid b ars or d el­
taic grow ths from
older b ar rem n an ts

St

sa n d , m edium
to v. c o a rse ,
m ay b e pebbly

solitary (thcta) or
grouped (pi) trough
c ro ssb e d s

d u n e s (lov/cr flow
regim e)

Sp

sa n d , m edium
to v. c o a rse ,
m ay be pebbly

solitary (alpha) or
grouped (omikron)
plan ar cro ssb e d s

linguoid, tran sv e rse
b ars, sa n d w av es
(low er flow regim e)

Sr

sa n d , very
tine to c o a rs e
sa n d , very fine
to very co a rse ,
m ay be peubly
sa n d , fine

ripple m arks of all
types
horizontal lamination,
parting or stream ing
lineation
low angle (<10°)
cro ssb e d s

ripplos (lower flow
regim e)
p lan ar b ed flow
(I. and u. flow regim e)
sc o u r fills, c re v a s s e
sp lay s, an tid u n cs •

Se

erosional sc o u rs
with in traclasts

cru d e cro ssb ed d in g

sc o u r fills

Fcf

m ud

m assiv e, with fresh w ater
m olluscs

b ack sw am p pond
d ep o sits

Fm

m ud, silt

m assiv e, desiccation
crack s •

overbank or
d ra p e deposits

Gt

Sh

SI

of

65

CREGO
r z l Gm

C It K

ELMIRA

LOWER
WILKES

ASPHALT

NEW
Gp WILKES
UPPER

WILKES

5

Sh
Se
Sh

-1
<
tW

~~
a

k

Sp
Sh

CD

to

Sp
Sh
Sp

Figure 24.
Bedform lithofacies
a sso cia ted with the
Elmira outwash surface
4 ml

Sh

U
DNR

Ss

5 km

N

66

c l a s s i f i e d as proximal,
types

(Fig.

Donjek,

24,

Table

Platte,

recognized
PROXIMAL:

medial,

2)

distal,

and c o m p a r e d wi t h the Scott,

and Bi jo u Cr eek models.

in the p re s e n t

study are

(Crego and C - K gravel

textured,

poorly

boulders.

A flow till

mass

the C - K pit,

s ug ge s ti ng

depositional

facies.

(Fig.

both gra vel

sorted,

25)

Th e Crego

sand.

and include

site

(Fig.

This

26),

site

and

a g g r a di ng

sandy b e d f o r m s and b r o a d

S e d i m en ts

are

co nt a i n s

1)

There

finer grained,

is finer grained.

TRANSITI ONA L:

are

i d en ti fi ed

in

in cl u d e s cy cl i c a l
scour

fills.

2) b e t t e r

sorted,

and 3)

than proximal

characteristic

Co bb le s

are rare.

Asphalt,

Up pe r Wilkes,

Fac ie s at these pits

of b o t h medial

and p r o x i m a l

They

and New

are
sites.

are sm a l l e r and so mewhat b e t t e r s o rt ed

in p r o x i m a l pits.

No silt

identified.

(Elmira,

gravel pits)

of p l a n a r

lacust ri ne

is a h i g h e r p r o p o r t i o n of sand to gravel and

or cl ay dra pes

Gravel s

large

is d o m i n a t e d by Gp

c r o s s - s t r a t i f i e d to a mu c h great er deg re e

Wilk es

Grave ls

from an ice -c on ta ct

and clay drapes are

(Lower Wil ke s pit)

the la tt e r

but

pits.

and St l i t h o f a c i e s

pits.

is

is w i t h i n the G m facies at

tra ns it io n

silt up to 33 cm thick,

facies

This a s se mb l a g e

m od er a te a mo u n t s of i n t e r l a y e r e d

are c oa r s e

MEDIAL:

Principal

i d e n t i f i e d below:

pits)

d o m i n a t e d by G m and Gp li t ho fa ci es
con tai ns

or tr an si t i o n a l

than those

also ex hib it a g r e a t e r abundance

(G p ) and tr ou gh -c ro ss

beddin g

(G t ), rath er than

67

TABLE 2. Bedform lithofacies of gravel pits
on the Elmira surfaceDesignation

Comments

Site

Facies identified

Crego

Gm, Gp, Gt, Sh,
Sp, Fsc

Proximal

Elmira

Gm, Gp, St

Transitional Gm and Gp
predominate;
no silt

Asphalt

G m , G t , Gp,. St,
Sh, Sp

Transitional Gm, G t , St
predominate;
no silt; more
sand than
Crego, Elmira

C and K

G m , G p , Gt, Sh,
St, Fm, Fsc, Gms

Proximal

Gm predomin­
ates; silt,
clay drapes;
small flow
.till inclus­
ion in Gm

Lower
'Wilkes

Gp, St, Spr, Sh

Medial

Gp, St
predominate;
no silt

Upper
Wilkes

Gt, St, Gp,
Sp, Sh

Transitional Gp predomin­
ates ; no
silt

New Wilkes

r* _
r* a.
,_
U t , tap,
o
p, o
w

Transitional No silt

DNR

Sh, Sp, St,

Distal

Gm and Gp
predominate;
thick,
lacustrine
sandy silt

Thick,
fining up­
ward Sh

68

Figure 25. Sedim ents at the C and K gravel pit
(proximal), Mancelona.

69

Figure 26. Sandy bedforms at the Lower Wilkes
gravel pit (medial), Mancelona.

70

massive

gra ve l

sh ee t s

DISTAL:

(D N R g r a v el

(Gm).

pit)

Sediments

here are c o m p o s e d

al m o s t e x c l u s i v e l y of sand and granules.
do m i n a t e s

the pit

(Fig.

silt or clay layers,

27).

Large

c o n t a i n more

sandy bedforms

facies model

but o t h e r w i s e

bo u l d e r s
facies,

facies.

(G p ) lenses,

In general,
sheets

(Miall,

lens es

in di c at e

of silt

1972;

c r o s s - b e d d e d gravel
deep water

lenses a n d clay

r e p r e s e n t s d e p o s i t i o n of

1981).
that

rapid

from t r a n s p o r t during w a n i n g
C l a y d r a p e s and sand and

flood

silt

flow c o n d i t i o n s were h i g h l y

of p r o x i m a l

outwash environments

F r a s e r and Cobb,

1982).

b e d f o r m fac ie s at the Lower W i l k e s

silt at the L o w e r W i l k e s

except

gr av e l pit.

for th e
These

a v a r i e t y of bars and be df o r ms

shallow,

of Gm

f lo od stages.

is si m i l a r to the D o n j e k model,

wide,

2) d o m i n a n c e

(38 cm),

the Gm facies

t yp i c a l

The m e d i a l

rep re se nt

1) the p r e s e n c e of

and l o n g i t u d i n a l bars during

sta ge s

(Church,

include

representing overbank sediments

d e p o s i t i o n of b e d l o a d

variable,

g r a v e l pits

ex h i b i t many c h a r a c t e r i s t i c s

of t h i c k

4) p r e s e n c e

possibly

but no

th a n p r e d i c t e d by the Scott

coa rs e texture,

deposited during waning

gr av e l

-- Pr ox im al

i n d i c a t i v e of h i g h energy,

d e p o s i t i o n and,
drapes,

Th es e

and o v e r a l l
3) p r e s e n c e

scour fills,

are recognized.

INTERPRETATION AND COMPARISON

of pr o x i m a l

L i t h o f a c i e s Sh

braided

stream

site

a b sen ce

sediments

typical

(Fraser and Cobb,

for a
1982).

of

71

Figure 27. Lithofacies Sh at the DNR sand pit (distal), Kalkaska.

72

The di st a l

D N R gra ve l pit has c h a r a c t e r i s t i c s

both the P l at t e
s eq uen ces

and Bi jo u Cr ee k models.

of p l a n a r

sands

c r o s s - b e d d e d laye rs

(Sp).

by p e b b l e s
bases,

(Sh)

In places,

are

thick

are cap pe d by th in pla na r

A fining u p w a r d

is indic ate d

at the b o t t o m of some Sh units.

the de p o s i t s

of

On these

i n t er pr et ed as a b r a i d e d stream

syst em e x h i b i t i n g m a r k e d l y var ia bl e d i s c h a r g e wi t h
p er i o di c

f l oo di ng

exposure,
typical

areas

(Bijou C re ek model).

of b ro ad

of the Pl a t te

scour

fills are

facies model.

Elsewhere

in the

identified,

more

Areas of the pit

where ke y r e l a t i o n s h i p s might be e s t a b l i s h e d are not
exposed.

A parsimonious

a dist al
further

facies,

ana ly si s

p ro xi ma l

These

interpretations

awaiting

facies

range

in E l m i r a o u t w a s h

from coarse,

p o o r l y sorted,

m e l t w a t e r d ep o s i t s d o m i n a t e d by l o n g i t u d i n a l

bars to dis ta l

fine

stream d e p o s i t s

textured,

wel l-s or te d,

mapp ed as the

braided

d o m i n a t e d by sandy bedforms.

in b e d f o r m facies co m pl em en ts

and s u p p o r t s the

This

tex tu ra l

ana ly si s

i n t e r p r e t a t i o n that what was p r e v i o u s l y

Inner Port H u ro n Mo r a i n e c r es t

marks an e s p e c i a l l y

actually

im portant head of outwash,

grad ed to the e x t e n s i v e
Plain.

this site as

indicates that a de f i n i t e

in b e d f o r m facies exists

deposits.

change

wi t h de tai ls of

i d e n ti fi es

study.

In summary,
change

ap p r o a c h

which

is

E l m i r a surfa ce of the M a n c e l o n a

73
Paleocurrents

-- P a l e o c u r r e n t d i r e c t i o n s were

r e c o r d e d at

eight gra ve l pi t s

and c o n s i s t e d of 1) m e a s u r e m e n t

i m b r i c a t e d gr av e l

fabrics

(Rust,

1975),

of

and 2)

d e t e r m i n a t i o n of d i p d i r e c t i o n w i t h i n p l a n a r c r o s s - b e d d e d
sands,

b a s e d on s t e r e o g r a p h i c p lo ts

strike.

Paleocurrent directions

ice m a r g i n

in p r o x i m a l

of a p p a r e n t

are p e r p e n d i c u l a r

r e g i o n s and pa ra l l el
sandur

data

first ten de d to

that m e l t w a t e r

perpendicularly away
degrees

from the

tracts.

s i m i l a r c ur r e n t p a t t e r n s
We st C h i c a g o M o r a i n e

Paleodischarge
calculated

28).

ice margin,

right to ru n p a r a l l e l

s a n d u r ’s d i st a l

(Fig.

to

Th es e

flow

in the

(1982)

found

in v a l l e y trains p a r a l l e l i n g the

in Illinois.

-- P a l e o d i s c h a r g e es t im at es we re

to d e t e r m i n e w h e t h e r or not c a t a s t r o p h i c

d r a i n a g e occ ur re d.

A s s u m p t i o n s and d i f f i c u l t i e s

paleodischarge

a n a l y s i s have b e e n r e v i e w e d

(Briggs,

Mai zels,

1983;

1983a;

All m e t h o d s d e p e n d o n d i r e c t
for use

ice

to t h e n tu r n 90

the m a rg i n

F r a s e r and Cobb

to the

to the

m a r g i n along the axis of the
in di ca te

dip and

of

in de ta i l

Lord and Kehew,

1988).

or su r r o g a t e m e a s u r e m e n t s

in the e q u a t i o n Q = w * d * v, w h e r e Q =

discharge,

w = c h a n n e l width,

v = m e a n c ha n n e l
determined

ve locity.

difficulty

depth,

and

P a l e o d i s c h a r g e s we r e

for the E l m i r a s u rfa ce o v era ll

representative proximal
v a lu e s most

d = m e a n ch a n n e l

an d m e di a l

and

for

gra ve l pits.

Th es e

l i k e l y ar e g r e a t l y u n d e r e s t i m a t e d due
in d e t e r m i n i n g a c c u r a t e c h a n n e l widths.

to the
Where

/

'

A DIP DIRECTION OF
1 # IMBRICATED GRAVEL

S CURRENT DIRECTION SHOWN
rn BY CROSS-BEDDING

Figure 28. Paleocurrents on th e Elmira surface.

75

applicable,

sl op e s w e r e a d j u s t e d

approximately

20% a n d

b r a i d e d streams.

for

isost ati c

r e b o u n d of

for an a s s u m e d s i n u o s i t y of

Methods used

1.1

for

in this s t u d y are

d i s c u s s e d b r i e f l y below.

Slope - discharge
L e o p o l d and W o l m a n
con s t a n t di sch ar g e,
than those

(1957)

braided

that meand er,

two was a p p r o x i m a t e d

method s

demonstrated

st re am s have s t e e p e r

S = tangential
some

* Q

o.MH

slope.

braided

p r e d i c t e d range,

slopes

by the equation:
-

Although

at a

and that the b o u n d a r y b e t w e e n the

S = 0.06
wh er e

that,

strea ms

exist

outsi de

the e q u a t i o n p r o v i d e s

determining minimum bankfull

of this

a method

discharges

for

of b r a i d e d

sy st em s on a g i v e n slope.
Cheetham
equation

(1976,

1978)

c a l c u l a t e d the r e g r e s s i o n

for L e o p o l d and W o l m a n * s

d e r i v e d the

b r a i d e d s t r e a m s and

f o l l o w i n g r el at io ns hi p:
Qbf = 0. 00 0 5 8 5

w he re Qbf = b a n k f u l l
minimum estimates

discharge.

Both equations

o n l y and a s s u m e no o v e r b a n k

Brig gs m e t h o d
Briggs

(1983)

presents

determining paleodischarge.
o n l y ch a n n e l
e s t i m a t es

* S~2,01

slope,

of p e r c e n t

flow.

#2

s e ver al me tho ds
His

for

sec on d m e t h o d

particle diameter
silt and clay

are

(Dg^),

re q u i r e s

and

in the c h a n n e l

76
perimeter.
diagram.

Velocity
D ept h

is d e t e r m i n e d

from S u n d b o r g ’s

is c a l c u l a t e d u s i n g the M a nn i n g
D = ( V * n

equation:

) 1,67

\T T

wh ere

n = M an ni ng

Ma nn i ng

r ou ghn es s

roughness,

V = velocity,

and D = depth.

is d e t e r m i n e d using S t r i c k l e r ’s

formula:
0 .1 7

n = 0.0132
Ch an ne l w id th

is c a l cu l a t e d u s in g

D 94
S c h u m m ’s expression:
- I.OQ

W = (255
wh er e W = wi dt h and M
perimeter.

Estimates

the n c o m bi n ed
ca l c u l a te

= % silt

* M

) D

and clay in the channel

of depth,

velocity,

and w i d t h are

in the e x p r e s s i o n Q = W * V * D t o

discharge.

• M a iz el s m e t h o d s
Ma i ze ls

(1983a)

paleodischarge

pr es ent s

techniques,

#1 and #2

a t h o r o u gh rev ie w of

i n c l u d i n g a n u m b e r of

si mp l i f i e d e q u a t i o n s

r e q ui ri ng

di a m e t e r and slope.

U n f o r t u n a t e l y these eq u a t i o n s

es ti ma te s
must

for cr iti cal

be m u l t i p l i e d

sp ec if ic di sc ha rg e

by chann el

cri ti ca l d i s c h a r g e (Qc).
pit,

w her e a c o n s e r v a t i v e

possible,

inputs of on l y p ar ti cl e

are d i s c u s s e d

Ex c e p t

for the L ow er Wilk es

es ti m a te

D e r i v a t i o n of the

in M ai ze ls

(q c ), wh ic h

w i d t h to p r o v i d e total

widt hs were de r i v e d usi ng

d e s c r i b e d above.

give

(1983a):

of ch ann el w i d t h was
S c h u m m ’s e x p r e s s io n
foll ow ing equa ti ons

77
Ma i z e l s m e t h o d #1

-- S.S2

(C h e z y equation!

Di/2,

S1/3

M ai ze l s m e t h o d

#2

(Manning - S t r ic kl er

equation)

a/ C. 0.2.<l3/2 l l . l t » 2 1 0 5 ( ^ ) 1
*

s-----------

where qc = cri ti ca l
in this

study),

Excep t

specific discharge,

and s = channel

for L eo p o l d and W o l m a n ’s technique,

from 415

paleodischarges
if widths

- 915 m"* sec'/(Table

Eve n so,

in Crego values,

that are m u c h too

we r e not d e p o s i t e d

Likewise,

Wide

p r o b a b l y due

large

to

(322 m).

s u g ge st in g that the se d im en ts

from other

including S c o t l a n d

o b se rv ed

in a s s o c i a t i o n wi t h c a t a s t r o p h i c

Th es e va l u e s are also c o m p ar ab le

paleodischarges

to

formerally glaciated

regions,

(1040 - 3120 m1 s e c / ; Maizels,

and the C a n a d i a n R o ck ie s
1975) .

3).

these data tend to c o nf i r m t e x t u r e and

be df or m analysis,

drainage.

in agreement,

for the L ow er Wi l k e s pit are c o m p a r a b l e

occur

width estimates

(

esti ma te s

from S c h u m m ’s r e l a t i o n s h i p are used.

discrepencies

size

slope.

from the E l m i r a surfa ce are g e n e r a l l y
ranging

D = c la st

(1000

1982)

- 6000 m3 s e c / ; Clague,

78

TABLE 3. PALEODISCHARGE ESTIMATES,
Site
Elmira
surface
overall

Crego

Lower
Wilkes

Leopold and
Wolman

Maiael
HI

Maiael
H2

Cheetham

Briggs
#2

Q=10,600
m3 s q c '1

Qbf=610
m3 sec - /

Qb=415_ qc=2.8 qc=6.1
m3 sec*/ Qc=429 Qc=915
m 3 sec“1 m3 sec-/

Q=695
J
-1
ra sec

Qbf=55
m 3sec'/

Qb=2450 qc=8 .7 qc=12.6
m3sec/* Qc=2800 Qc=32
m3 secw * mJsec *

Q=210
nr3 sec~l

Qbf=l_9
m3 sec"*

Qb=30
m,3sec,

♦using width from Schumm's expression

qc=.6
Qc=30
m3 sec*;
Qc = 6 .1
m 1sec*'

qc= .6
Qc=32
m3 sec*;
Qc=6.5
3
-1
mJsec

79

Till

a s s o c i a t e d w i t h the

P i n k till

(5 YR

l o c a t i o ns

al on g the

Crego

tills,

7/3,

Ta bl e

32 N . , R.

4 W.).

dry)

crops

out

in s c a t t e r e d

Inner Port H u r o n apex
5),

northernmost gravel

I nn er Po r t H u r o n C o m p l e x --

pit

and

(W o o d l a n d and

is best e x p o s e d at C r e g o ’s

(NE1/4,

NW1/4,

Characteristics

1) J u x t a p o s i t i o n of till
gravel.

SW1/4,

of this

sec.

till

15,

T.

include:

and g l a c i o f l u v i a l

sand and

2) C o n t o r t e d g l a c i o f l u v i a l be dd in g s l o p i n g toward
de ep cl os e d d e p r e s s i o n s i m m e d i a t e l y a d j a c e n t to the
exposure.
3) P r e s e n c e of b ou ld er s at the top of the exposure,
p o s s i b l y su gg e s t i n g d u m p i n g of m a t e r i a l s from
ad j a c e n t st ag n a n t ice.
4) V e r t i c a l c o n t ac ts b e t w e e n till and g l a c i o f l u v i a l
sediments; d r a g f o l d i n g i n d i ca te s till m o v e d
d o w n w a r d r e la t iv e to s t r a t i f e d layers.

K ee b l e
assemblages
meltwater

(1970)

and Shaw

(1972)

attributed

to d e p o s i t i o n of s u p e r g l a c i a l

sediments

into m o u l i n s

at the C re go

site

ind ic at es

in a s im i l a r

fashion.

th at

si mi la r

till

and

or crevasses.

E v id en ce

till here was

deposited

S E D I M EN T S A S S O C I A T E D WI T H THE
POS T INNER P O R T H U R O N ZONE
The Post
proximal

to the

Se d i m e n t s
gravel,

Inner Port H u r o n

zone

In ne r Port H u r o n

is l o c a t e d

ice-contact

are p r e d o m i n a n t l y g l a c i o f l u v i a l

w i t h le ss e r a m oun ts

of till

just

slope.

sand

and

and l a c u s t r i n e

silt

an d clay.
Few e x p o s u r e s

of g l a c i o f l u v i a l

de p o s i t s

w e r e located.

80

A small e x p o s u r e
SE1/4,

T.

in o u t w a s h

31 N . , R.

s u rf ac e A

5 W. ) e x h i b i t s

grave l wi t h w el l - s o r t e d ,

( Ch.

3, NE1/4,

s t r a t i f i e d sa n d and

r o u n d e d cobbles up to

10 cm in

b-diameter.
The A n t r i m C o u n t y Road C o m m i s s i o n grav el
1/4,

NW

1/4,

complexly

sec.

T.

30 N.,

fo ld e d l a c u s t r i n e

with overlying
gravel

33,

(not

sh own

6 W . ) contains

s i l t / c l a y layers

in diagram).

(Fig.

taken

obvious anticline

O r gan ic m a t t e r

l ay er of this

a r a d i o c a r b o n date of

12,960

from the

29)

re co ve re d

la cu s t r i n e c l a y yi el de d

+ 350 yrs.

B.P.

(TX - 6151).

l o we r part of a small

yet

2 m below the top of the e x p o s u r e

the east b a n k of the pit

(Fig.

29).

r a d i o c a r b o n date and an a n al ys is
pr i n c i p a l

(NW

u n c o n f o r m a b l e , u n d e f o r m e d o u t w a s h sand and

from a d i s t i n c t i v e

Sa mp l e s we r e

R.

pit

successive

along

B as ed on the

of st ra ti gra phy ,

three

events are recognized:

1) L a c u s t r i n e and or gan ic
12,960 yrs. B.P.

m a tt er d e p o s i t i o n c.

2) D e f o r m a t i o n of l a c u s t r i n e deposits.
3) I n i t i a t i o n of fosse m e l t w a t e r drainage,
d e p o s i t i o n of o u t w a s h sediments.

and

I n t e r p r e t a t i o n and s i g n i f i c a n c e of this s t r a t i g r a p h y is
discussed

in C h a p t e r

Two m a i n till
Post

7 W.)

7/3,

e x p o su re s

were

id ent ifi ed

in the

sec.

28 N.,

Inner Por t H u r o n zone.

Plum Valiev
R.

4.

dry)

s i t e : (SE1/4,

This
ba sa l

SW1/4,

site c o nt ai ns
till

6, T.

two tills:

at an al t i t u d e

1) a b r o w n

about

(10 YR

66 m b e l o w the

S75E

Slump

LACUSTRINE SILT; RIPPLE
DRIFT CR O SS LAMINATION
liS T I
lir-lj

SAND

LACUSTRINE SILT; MASSIVE,
COLOR BANDS

Figure 29. Stratigraphy at the Antrim
County Road C om m ission gravel pit.

82

crest of the Inner Port H u r o n
an overl yin g d ep o s i t

ice- con tac t

containing alternating

sa ndy s tra ti fie d till and sand lenses.
tills are se pa ra te d by plan ar

1971,

Hartshorn

and

studies

1972),

(1958),

Kaye

and Ri eck

and 2)

layers of

In places,

the two

sands up to 35 cm thick.

Flow till has been re co gn i z e d
others,

slope,

and d e s c r i b e d by,

(1960),

(1976).

recog niz e nine c r i t e r i a

Boulton

among

(1968,

Collect iv el y,

for i d e n ti fy in g

these

flow

till:
1) In te rf in ge ri ng of the
gl aci ofl uvi al sediments.

flow till unit wi th

2) O r i e n t a t i o n of str iat ed pebble s par al le l
d i r e ct io n of movement.

to the

3 ) Pre se nc e of sandy lenses and hor izo ns
in cor por ate d wi th i n the deposit.
4) Sharp p l a n a r contac t wi t h su b ad ja ce nt materials.
5) Smooth, ver ti ca l
exposures.

faces

in re la ti v e l y

fresh

6) O v e r c o n s o l i d a t e d natu re wh en dry.
7) Close a s s o c i a t i o n w i t h

ice- con tac t

slopes.

8) Presenc e in high er t o p og ra ph ic p o s i t i o n s withi n
the landscape.
9) Till

fabrics par allel

The upper till exh ib it s
orientation,

to ma x i m u m surfac e
interfingering,

and sandy lenses.

absent.

sands

but smooth o v e r c o n s o l i d a t e d

The de p o s i t caps a small

to the Inner Port Hu ro n
c r it er ia #7 and #8.

ridge

ice -c on ta ct

On all

pebb le

Sharp p l a n a r co ntacts

also exist be tw ee n this till and the p l an ar
me nt io ne d above,

slopes.

1/2 mile proximal

slope,

these bases,

facies are

sat is fy in g

the up per till

83

is id ent if i ed as flow till.
Be cau se of the li mit ed d a t a available,
these dep os it s
may re pr ese nt

is d if fi cu lt

to determine.

the

age of

The

lower till

s ubg lac ia l d e p o s i t i o n dur in g ad van ce

Ou t e r Port H u r o n position,

wi t h s u b s eq ue nt

to the

flow till

de p o s i t i o n dur in g deglaciation.
Si mp s o n gravel p i t : (SE1/4,
W.)

Here,

NE1/4,

a sandy till e x po se d

sec.

sediments,
presence

1)

T.

29 N.,

R.

in a n o r t h w e s t - s o u t h e a s t

tren di ng d i s i n t e g r a t i o n ridge di sp l a y s
c h a r a ct er is ti cs:

11,

the

follo win g

in t e r fi ng er in g wi th g l a c i o fl uv ia l

2) o r i e n t a t i o n of s t r i a t e d pebbles,

of sandy lenses and horizons,

4)

3)

high

to p o g r a p h i c p o s i t i o n and 5) close a s s o c i a t i o n wi t h the
Inner Port H u r o n

ic e- contact

slope.

On these bases

it is

i n te rp re te d as flow till.

TI LLS A S S O C I A T E D WI T H FL U T E D U P LAN DS
Till

is w i d e s p r e a d

in fluted up l a n ds p r o x i m al

the Post

Tnner Port Huron zone;

e x am in ed

in detail:

1) B a rk e r C r e ek
8 W. )
2) T or ch Lake
8 W. )

four e x p o s ur es were

( N W 1 / 4 ,S E 1 / 4 , sec.

(S E 1 / 4 , N E l / 4 , sec.

3) Z i m m e r m a n Road
R. 8 W. )

31,

33,

(S E 1 / 4 , N E l / 4 , sec.

4) T hu mb Lake Road
N . , R. 5 W . )

Wit h the e x c e p t i o n of #4,

to

T.

28 N.,

R.

29 N . , R.

4, T.

(S E 1 / 4 ,S E 1 / 4 , sec.

all are b ro wn

T.

12,

in c o l o r

28 N . ,

T.

32

(10 YR

7

84
6/3,

7/3,

dry;

Table

5) and l oc ate d south and east

Ske ge mo g and T o r c h Lakes.

Melhorn

(5 YR 7/3,

dry)

till as "Valders

consistent

stratigraphic

are r e c o g n i z e d

T h u m b Lake

(1956)

of

i de nt if ie d pink
till."

No

r e l a t i o n s h i p s am on g the tills

in this study.

m i n e r a l o g y are d i s c u s s e d

Texture,

later

color,

and clay

in this chapter.

S U R F I C I A L S E D I M E N T S A S S O C I A T E D WI T H THE
O U T E R PORT H U R O N COMPL EX
On l y two
gravel pits)
at the time

large e x p o s u r e s

field study was conducted.
sand and gravel,

glaciolacustrine

clay

till.

ou tc ro ps

Pr i n c i p a l

Fleming Fa r m gravel
4 W.).

and Ro s e n b u r g

Rd.

e x is te d w i t h i n the O ut er Port H u r o n feature

mostly glaciofluvial

R.

(Fleming

Here,

in the

De po si ts

are

w i t h some

s ou th and absen ce of basal

are di s c u s s e d below.

p i t : (NE1/4,

NE1/4,

a c h o c o l a t e - b r o w n till

sec.

11,

T.

31 N.,

(10 YR 6/3)

cores

a n o r t h - s o u t h o r i e n t e d ridge c o m p o s e d of d e f o r m e d
glaciofluvial

deposits;

these lat te r sedi me nt s d i s p l a y a

u n i f o r m c o n v e x - u p w a r d curvature.
The

1)

li ne a r natu re of the

glaciofluvial
str at i f i e d

sediments,

sediments,

3)

ridge,

2) d e f o r m a t i o n of

j u x t a p o s i t i o n of till and

and 4) p r e s en ce of mul ti pl e

d i s i n t e g r a t i o n ridges of s i m i l a r size and o r i e n t a t i o n
nearby

in dicate that these

within crevasses

sed im en ts were d e p o s i t e d

in st ag n a n t

ice

(Kaye,

1960;

Keeble,

1970) .
Ro s en bu rg R o a d gravel
N.,

R.

7 W.).

p i t : (SE1/4,

This pit

NE1/4,

sec.

13,

T.

is l oc at ed near the p r o x i m a l

27
edge

85

of the O u t e r Port H u r o n C o m p l e x an d c o n t a i n s
highly deformed coarse
lacustrine
clay

glaciofluvial

silt and clay lenses.

is e x p o s e d at the s o u t h e r n

Deformation

sand and gravel,

and

A 3 m thick lacustrine
face of the pit.

s t r u c t u r e s a p p a r e n t l y are r e l a t e d to an

adjacent closed depression
interpreted

boulders,

similar

12 m deep.

sediments

Shaw

in E n g l a n d as

(1972)
ice-contact

s t r a t i f i e d drift.
Other

Exposures: Excavations

Bu i l d i n g "

(NE1/4,

stratified
contact

sec.

sand and

slope,

21,

g ravel

T.

29 N.,

evidence

m a r g i n a l d e p o s i t s w i t h i n the

6 W.)

Th i s

la ye r s

reported

altitudes

outcrops

of

ice-

from

are p r o b a b l y

are l i s t e d below:

lacustrine deposits

T h e y are best e x p o s e d

NE1/ 4,

27 N.,

26,

T.

sand an d g r a v e l u n i t

R.

(bedding

chocolate brown

5 W.
5 W.
5 W.
6 W.
6 W.
8 W.
W.

cr o p out at s e v e r a l plac es

eas t of Ka lkaska.

massive,

o ut cr op

I n n e r an d O u t e r Po r t Hu ro n

1)
S W 1 / 4 ,NE1/4, sec. 10, T. 30 N . , R.
2)
NW1/4, S W 1 / 4 , sec. 11, T. 30 N., R.
3)
SW1/4, N W 1 / 4 , sec. 14, T. 30 N., R.
4)
S W 1 / 4 ,S E 1 / 4 , sec. 32, T. 28 N . , R.
5)
S E 1 / 4 ,N W 1 / 4 , sec. 17, T. 27 N . , R.
6)
SE1/4, S E 1 / 4 , sec. 32, T. 26 N . , R.
7) El/2, N W 1 / 4 , sec. 15, T. 25 N., R. 8

sec.

ice-

d e p o s i t s as well.

Other glaciofluvial

Thick

showed

for the a b u n d a n c e

logs at c o r r e s p o n d i n g

glaciofluvial

R.

the crest.

t h i c k sa n d and gr av e l

n e a r b y well

"Mancelona Water

in the O u t e r Port H u r o n

30 - 40 m b e l o w

provides additional

features;

for the

7 W,

where

in the NW1/4,
a 30 cm t h i c k

indistinct)

lacustrine

overlies

a

clay mo r e t h a n two

86
mete rs

thick.

recognized.
proglacial

No b an din g
T h e s e clays

lake that

grade vertically,
tough,

clay

a p p a r e n t l y were d e p o s i t e d

formed b e t w e e n the

the O u t e r Port H u r o n
Melhorn writes

or l a m i n a t i o n of the

ic e - c o n t ac t
(1954;

p.

slope

81)

s l i g h tl y p e b b l y blue till

(Melhorn,

break,

below."

1954).
clays

into

No

the

s i mi la r

re l a t i o n was o b s e r v e d along the O u t e r Port H u r o n
contact

slope

in the

e x p o s u r e of till

for

changes

Initially,
construct

p i l es

and,

(see next

network

T he se p il es
the

found more

Fo rt unately,

Port H u r o n apex.

section),

locat ed

2)

1)

stone pile

s i mi la r to that
are

r e st ri c t e d

ice-contact
than

in o r d e r

slope,

this p a t t e r n

is

is e v i d e n c e

to

on the
to a v e r y

however,

1 k i l o m e t e r dis ta l
itself

co mb i n e d w i t h b o u l d e r d i s t r i b u t i o n s

observa ti on s,

5) was

in the O u t e r Port H u r o n

of stones we r e

a sampling

n a r r o w zone a l o n g

crest.

Table

small

f ie ld e x a m i n a t i o n of outcrops.

E l m i r a surface.

none were

ice-

o n l y one

c h a n g e s were d e t e r m i n e d u si ng

boulder distributions
and 3)

till,

south of the O u t e r

facies

C o m p l e x -- Fa c i e s

mapping,

In fact,

( Cre ig ht on Road

recorded anywhere

Evidence

study area.

in a

ice m a r g i n and

" (l ac us tr in e)

w i t h no n o t i c e a b l e

is

and

to the
si gn ificant,

and

field

for a facies c h a n g e

from coarse

to fine distally.

Boulder distribution

-- L ar ge

diameter)

of b o u l d e r s

and groups

0.5 m b - d i a m e t e r w i t h i n

bo ul d e r s

100-150

( >1.0

(3 or more

m b-

boulders >

m of one an ot he r)

are

87

c o n c e n t r a t e d a l o n g n a r r o w zones at the crest of
co n t a c t

slo pe s m a r k i n g

distributions
superglacial
d u ri ng

heads of o u t w a s h

are b e l i e v e d to resu lt
boulders

id en t i f i e d

(Blewett and Rieck,

1987)

changes,

ice m a r g i n a l

ch an ge s

positions,

and

2)

3)

positions,

in this

b a s e d on t e x t u r a l

and stone piles,

in e s t a b l i s h i n g

In a si mi l a r

distribution data presented
faci es

ice m a r g i n

in n o r t h e r n M i c h i g a n

and u s e d

stag nat io n.

These

S i m i l a r bo uld er

c o n c e n t r a t i o n s we r e

ice ma r g i n a l

15).

from d e p o s i t i o n of

by mass w a s t i n g at the

final de g l a c i a t i o n .

delimiting

(Fig.

ice-

facies

and v e r i f y i n g

fashion,

bo ul de r

study

1) v e r i f y

analysis

of gra ve l

help to i d e n t i f y

pits

ice ma r g i n a l

su ppo rt the s t a g n a t i o n - z o n e h y p o t h e s i s

for final d e gl a ci at i on .
An anomalous boulder

concentration

the base of the A l b a East t e r r a c e
the O u t e r Por t H u r o n
observed
NE1/4,

ic e- c o n t a c t

(Ch.
slope.

is l o c a t e d along
3),

proximal

It

is best

i m m e d i a t e l y south of the A l b a A i r p o r t

sec.

31,

T.

30 N . , R.

c r y s t a l l i n e b o u ld er s,
c on s t ru ct ion ,

5 W.),

to

(SW1/4,

wh er e mo r e t h a n 50

a p p a r e n t l y e n c o u n t e r e d d u ri ng

are p i l e d a lo ng A r t h u r Lane.

road

M a n y other

bo u l d e r s are n e a r l y bu r ie d by s u r r o u n d i n g g l a c i o f l u v i a l
sand and gravel,
Significance

w i t h o n l y the u p p e r

of this site

is d i s c u s s e d

S i m i l a r c o n c e n t r a t i o n s are

located

sec.

and NE

T.

3, T.

30 N.,

31 N . , R.

4 W.

R.

5 W.,

10-20 cm exposed.
in C h a p t e r 4.

in the NW
1/4,

1/4,

NW 1/4,

NE

sec.

1/4,
19,

88

SOILS
Soils

are a u s e f u l me an s

for d e t e r m i n i n g

p a t t e r n of s u r f i c i a l p a r e n t ma t e r ia l.
ar e a are p r e d o m i n a n t l y sand,
san d

in te xt ur e

c l a y loams are
or l a c u s t r i n e

(Table 4).
rare

Soils

san dy loam,
Loams,

te x t u re and
in the

and

l oa my

cl a y loams,

but ma y be us ef u l

study

an d silty

in di ca t o r s

of till

d e p o s i t s as d e m o n s t r a t e d below:

a. N e s t e r sil ty clay loam: ma y d e l i n e a t e M e l h o r n ’s
V a l d e r s till n o r t h of the Inner Port H u r o n apex.
b. B e r g l a n d loam; Be r g l a n d cl a y loam: m a y de l i m i t
l a c u s t r i n e c l a y in the O u t e r Port H u r o n feature.
c. Ba rk e r
uplands.

loam:

in te r p r e t e d

d. C h e s t o n i a si lt y clay
l a c u s t r i n e (?) dep o si ts

Soils along
to be

as bro wn till

loam: i n t e r p r e t e d as
in A n t r i m County.

the crest of ice m a rg in al

finer t e x t u r e d than do mo re dist al

d i s t r i b u t i o n p r o b a b l y ref lec ts
silt and cl a y

in fluted

positions

soils.

an a b u n d a n c e

in t he se p r o x i m a l deposits,

tend

This

of ov e r b a n k

as we ll

as fine

s e di me nt d e p o s i t i o n w i t h i n an o p e n gravel m a t r i x during
waning

flood c o nd it io ns .

lacustrine
ot her

silt and clay,

fine-textured

proximal

re gi o n s

sta gna ti on,

i n t e r pr et in g

flows,

ic e- c o n t a c t

flow and a b l a t i o n tills,

and

se di me nt s are also c o n c e n t r a t e d

m a r k i n g h ea ds

c h a r a c t e r i s t i c s are
marginal

D e br is

typical

of outwash.

these

of areas e x p e r i e n c i n g

and p r o v i d e

soil p a t t e r n s

All

a use fu l

basis

in the study area.

in

ice

for

89

TABLE 4. SOILS OF THE STUDY AREA.
County

Charlevoix

X
w
a

T
o
u
►7

Principal
Soil Complexes
or Associations

Principal
Soil Series

Surface
Soil
Texture

KalkaskaLeelanau

Kalkaska
Leelanau

sand
loamy sand

LeclanauEmmet

Leelanau
Emmet

loamy sand
sandy loam

MancelonaEast Lake

Mancelona
East Lake

loamy sand
gravelly
loamy sand

Alpena-KivaEast Lake

Alpena
Kiva
East Lake

gravelly
sandy loam
to gravelly
sand

o
cc
D
X

H
O

Antrim
(proximal)

KalkaskaMontcalm

Kalkaska
Montcalm

sand
loamy sand

n£
to
2
2

Antrim
(distal)

KalkaskaEast Lake

Kalkaska
East Lake
Rubicon

sand
gravelly sand
sand

Kalkaska
(proximal)

(old survey)

Kalkaska

loamy sand

Kalkaska
(distal)

(old survey)

Rubicon
Grayling

sand
sand

Antrim
(proximal)

KalkaskaMontcalm

Kalkaska
Montcalm

sand
loamy sand

Antrim
(distal)

KalkaskaEast LakeKarliu

Kalkaska
East Lake

sand
gravelly loamy

Karlin
Rubicon

loamy fine
sand
sand

OC

POST
INNER
PORT
HURON
ZONE,

OUTER PORT
HURON COMPLEX

CU

cnnH

Kalkaska
(proximal)

(old survey)

Emmet

sandy loam

Kalkaska
(distal)

(old survey)

Kalkaska
Emmet

sandy loam
sand

Antrim/
Charlevoix

KalkaskaMontcalm

Kalkaska
Montcalm

sand
loamy sand

Kalkaska

(old survey)

Kalkaska
Emmet

loamy sand
sandy loam

Sources: Veatch et al.
and Buchanan (1978) .

(1927); Alfred and Hyde (1970); and Larson

90
T E X T U R E AN D L I T H O L O G I C C O M P A R I S O N OF
TIL LS FROM THE STUDY A R E A
The v a r i a b l e d i s t r i b u t i o n and rel at iv e p a u c i t y of
till out cr op s

does not p r o v i d e an ade qu at e basis

det ai le d till

analysis.

Texture,

m i n e r a l o g y are,

however,

pur po ses

5).

(Table

s ig n i fi ca nt
di am i c to ns

li th ol og i c al

of 1) color
re present

of large clas ts

differences

Tills were

(pink vs.

brown)

the u p p e r m o s t

and clay

p r e s e n t e d for d e s c r i p t i v e

An a l y s i s

sampled.

color,

for

till

show ed no

among the

sub di vi de d

few

on the basis

and 2) w h e t h e r they
in the area

(high or low

p r o b a b i l i t y ).

Texture and c o r r e l a t i o n of tills

- T e x t u r e was

plotte d on a t e r n a r y d i a g r a m to i n v e s ti ga te po ss i b le
sample g r o u p i n g s
c o n c e n t r at ed

(Fig.

in the

in part to the

c on ta in in g

Re d till

s a mp le s are

lo we r- m id dl e part of the diagram,

restricted geographic

samples were taken,
B ro wn sampl es

30).

and are

se pa ra te

area from w h i c h the

likely from the

into two di st i n c t

same deposit.

grou ps

1) the C r e i g h t o n R d . , B a r k e r Creek,

Va l l e y tills,

a n d 2) the Zimmerman,

Fleming deposits.

T o r c h Lake,

The Z i m m e r m a n and T o r c h Lake

and Plum
and
samples

were ta ke n less th a n 1 km apart at s i m i l a r a l t i t u d e s
and 210 m,
deposit.

re sp ec ti ve ly )

and are p r o b a b l y

This c o n c l u s i o n

mineralogy data
Cr ee k samples

(Table 5).

due

(198

from the same

is s u p p o rt ed by co lo r and clay
The Pl u m V a l l e y and Ba r k e r

also d i s p l a y s im il ar texture,

but

the

TABLE’5. COLOR AND CLAY MINERALOGY OF PRINCIPAL TILLS.
o

Sample
name
Barker
Creek

Woodland

Munsell
dry

color
dry

1

10YR 6/3

pale
brown

10YR 7/3

very
pale
brown

61

102

.598

B

2
3
4

1-0YR 6/3
10YR 6/3
5YR 5/3

10YR 7/3
10YR 7/3
reddish 5YR 6/3
brown

53
31
23

03
83
20

.630
.373
1.150

B
B
R

26
44
20
41

10 2.600
25 1.760
25 • .800
30 1.367

R
R
R
R

45
21
24

.7.78
1.667
1.875

R
R
R

19
27
36
41
22
27
22
42

1.211
.556
.583
.659
1.000
.852
1.227
.762

R
R
R
R
R
R
R
B

64

.641

B

25
104

.680
.538

B
B

37
66
30

77
121
56

.480
.545
.536

B
B
B

28

64

.438

B

30

50

.600

B

45

55

.810

B

45
53
30

79
62
64

.570
.855
.469

B
B
B

46
30

85
56

.541
.536

B

ill

Woodland
02

5YR
5YR
5YR
5YR

Woodland
03

9
10
11

5YR 5/3
5YR 5/3
5YR 5/3

brown

20 10YR 5/3

1

21 10YR 5/3
22 10YR 4/3

brown/
dark
brown

V.

23 10YR 4/3
24 10YR 4/3
Creighton 25 10YR 5/3

Torch
Lake
Plum
Valley

6/3
6/3
7/3
6/3

5YR 7/3
5YR 7/3
5YR 6/3

5/3
5/3
5/3
5/3
5/3
5/3
5/3
5/3

12 5YR
13 5YR
14 5YR
15 5YR
16 5 YR
Crego
17 5YR
10 5YR
Zimmerman 19 10YR

Fleming

5YR
5YR
5YR
5YR

5/3
5/3
5/3
5/3

5
6
7
8

Thumb
Lake

Brown/
Red

color
moist

7A* 10A* 7/10A

0

Munsell
moist

brown

SYR
5YR
5YR
SYR
5YR
5YR
5YR
10YR

7/3
7/3
7/3
7/3
7/3
7/3
7/3
7/2

10YR 7/3
10YR 7/3
10YR 6/3
10YR 6/3
10YR 6/3
10YR 7/2

26 10YR 5/3

10YR 6/3

27 10YR 5/3

10YR 7/3

20 10YR 5/3

10YR 6/3

29 10YR 5/3
30 10YR 5/3
31 10YR 6/4

10YR 6/3
10YR 6/3
yellow­ 10YR 7/3
ish brown

32 10YR 6/4
33 10YR 6/4

10YR 7/3
10YR 7/3

light
reddish
brown

pink
light
reddish
brown
35
pink
35
45
light
reddish
brown
23
pink
15
21
27
22
23
27
32
light
gray
41
very
pale
brown
17
56
pale
brown

light
gray
pale
brown
very
pale
brown
pale
brown
very
pale
brown

♦Peak counts minus background as determined by computer.

B

92

100 % CLAY

C re ig h to n R d.
T h u m b L ak e
B a rk e r Cr.
W o o d lan d #1
W o o d lan d # 2

Z im m e rm a n
F lem ing

100% SAND

T orch

W o o d lan d # 3

A

BROWN TILL

■

RED TILL

Figure 30. Soil textures of principal tills
in the study area.

100% SILT

93
e x p o s ur es
a lt it ud e
Ta bl e

are

fa rth er

(273 m vs.

5 sugges t

components

207 m,

(10 km)

that these

and F l e m in g

24 km from ot her

s am pl es

such a d i s t a n c e

and d i f f e r

respectively).

in

Data

from

samples may represent

of the same deposit,

C r e i g h t o n Rd.

a c ro ss

apart

however.

F a r m tills

The

re m a i n i n g

are b o t h mo r e than

in t h e i r group.

Correlation

is sp ec ul a t i v e .

Clay mineralogy - Thirty-three

till

sampl es

from

11 sites

were a n a l y z e d to d e t e r m i n e

c o m p o s i t i o n of cl a y minerals.

Preparation

(no date;

fo l l o w e d Glass

resul ts were
(Rieck,

i n t e r p r e t e d us in g

1976;

One goal
mi ne ra l

T ab le

r es e a r c h e r s

7/10 A n g s t r o m ratios

5).

of the a na ly si s was

differences
(Bretz,

see A p p e n d i x B) and

to

investigate

clay

b e t w e e n red and br ow n

tills.

1951;

Me lhorn,

Be rquist,

1953;

Past
1954)

i n t e r p r e t e d b r o w n and red ti ll s as Port H u r o n and V a ld er s
(G r e a t l a k e a n ) deposits,

r e sp ec ti ve ly .

B u rg is

(1977)

r e c o g n i z e d b r o w n Port Bruce t i ll s

and

G r e a t l a k e a n tills.

noted a higher

co nt e n t

Taylor

in Port H u r o n

Greatlakean

(Filer)

(1981)

(O rchard Beach)

till.

Monaghan

red Port H u r o n and
illite

till t h a n

(1988)

compared

G r e a t l a k e a n and Po r t H u r o n till a l o n g Lake M i c h i g a n and
r e p o r t e d no d i f f e r e n c e s

in c l a y m i n e r a l

co mp os it io n.
o

Most
ratios

>

red till
1.00,

ch l o r i t e c o n t e n t
<1.00

from the s t u d y a r e a e x h i b i t s

7/10 A

i n d i c a t in g hi g h k a o l i n i t e and
(Fig.

31).

suggesting higher

B r o w n till

ill it e amounts,

ratios

are always

but m o d e r a t e

1.0
FREQUENCY

10

5

|

R E D TILL- low probability of b e in g t h e u p p e rm o s t d e p o s it

H

R E D TILL- h ig h probability of b e in g th e u p p e rm o s t d e p o s it

[3

B R O W N TILL- low p ro b ab ility of b e in g th e u p p e rm o s t d e p o s it

[]]

B R O W N TILL- h ig h p robability of b e in g th e u p p e rm o s t d e p o s it

1
— i—
.5

1.0

1.5

2.0

—

I—

2.5

7/10 Angstrom d a y ratio

Figure 3 1 . Frequency diagram of 7 /1 0 Angstrom ratios for tills in th e study area.

95
ov e r l a p

(.5 to 1.0)

p r e cl ud es c le ar d i f f e r e n t i a t i o n

be t w e e n the two tills.

To c o m p l i c a t e matters,

tills come

from w i d e l y sc a t t e r e d

altitudes,

and m a y be of d i f f e r e n t

may be true for red tills.
in d i ca ti ons that

lo cations at v a ry i n g

Thus,

ages;

the

lat te r also

d e sp it e p r e l i m i n a r y

red and brown de po s i t s ma y be

based on 7/10 A n g s t r o m ratios,
till

b r ow n

sepa ra ted

acc ur at e u n d e r s t a n d i n g of

s t r a t i g r a p h y and m i n e r a l o g y awaits more de fi ni t i v e

study.

S um mar y
The

Inner and O u t e r Port H u r o n C o m p l e x e s are

c om po se d of t h i c k dr if t o v e r l yi ng a mod er at e
northwest-southeast
t o p o g r a p h y mi m i c s

relief,

li neated b e d r o c k surface.

Prese nt

b e d r o c k form n o r t h of Mancelona,

p o s s i b l y due to h i g h e r b e d r o c k r e l i e f and t h i n n e r drift
here than

in a re as

farth er south.

Indivi du al

va l u e s are hi gh es t to w ar d the north;
bec om e

g re at e r t o w a r d the south.

gravel units
along

the

exposed,

th i c k ne ss

avera ge va l ue s

Up p e r m o s t

fo r m w e d g e - s h a p e d dep os it s

sand and

ne ar l y 85 m thick

Inner and O u te r Port H u r o n crests.

Where

these u n i t s are u n q u e s t i o n a b l y g l a c i o f l u v i a l

or i g i n and are not
W i s c o n s i n a n till
Su r f i c i a l

sandy till.

One po ss i b l e p r e - L a t e

is id en t i f i e d at Rugg Pond.

se d i me n t s w i t h i n a re as m a p p e d as morai ne

(Leverett and Taylor,
c o ns is t of

in

ic e - c on ta c t

sand and gravel;

till

1915;

F a rr an d and Bell,

1982)

st ra t i f i e d drift and pr og la c i a l
is very l i mi te d in ext en t

and

is

us ua l l y

in the

fo r m of flow till.

are resting on a m o de ra te
towards the northwest,
ch an ge app ar en t

ki lo me te r wide
Huron

12,960

and 2)

zone pro xi ma l

to the

e x hib it a d i s t i n c t

and b e d f o r m analysis.

to the Inner and Out er Port

Inner Port H u r o n
All

feature are da te d at

of these d a t a

the Inner and O u t e r Port H u r o n
but

facies

slopes d u r i n g d e g l a c i a t i o n ; those

+ 350 y r s . B.P.

end mor ain es

1)

clays were d e p o s i t e d w i t h i n a one

ic e- con tac t

pro xim al

sedim ent s

rel ie f clay su rfa ce that slopes

fr om both t e x t u r e

T h i c k l ac us tri ne

Su r f i ci al

features

indicate that

are not classic

instead are c o m p l i c a t e d as se m b l a g e s

la ndforms that e v o l v e d

in a s s o c i a t i o n w i t h ab undant

me lt wa te r and s t ag na nt

ice d u r i n g

final deglaciation.

of

Ch a p t er

3

L AN D FO RM S A S S O C I A T E D WI TH THE
INNER AND O U T E R PORT H U R O N CO MP LE XE S

Pr in cip al
the

1)

l a n d f o r m units

r e c o gn iz ed

Inner Port H u r o n Complex,

Plain,

2) Post

Complex,
valley s

(Figs.

3) O u t e r Port Huron

fluted uplands and a s s o c i a t e d th r o u g h
4,

th ro ug h va ll ey s

study are

inclu din g the Ma n c e l o n a

Inner Port H u r o n zone,

and 4)

in this

32).

Fluted uplands and a s s o c i a t e d

are not d i s c u s s e d

they are a n c i l l a r y to the

study,

field wor k was ca rr ie d out

in detail

b ec au se

1)

and 2) lit tl e de ta i l e d

in these areas.

B e d r o c k / l a n d f o r m r e la ti on sh ip s
As d e s c r i b e d
relief

the undulating,

(150 - 245 m) b e d r o c k surface

sub cr o pp in g
Alba,

in C h a p t e r 2,

li ne a r lowlands,

ex hi bit s

high

four

n am ed the Kalkaska,

Darragh,

and C h a r l e v o i x v a ll ey s that trend e i t h e r east -w es t

or n o r t h w e s t - s o u t h e a s t

(Fig.

6).

We s t of the st ud y area

are broad b e d r o c k lo wl an ds a s s o c i a t e d w i t h G r a n d Traverse
Ba y and T or ch and Elk lakes.
Figu re

33 shows that both the Inner and O u t e r Port

Huron Complexes
pattern.

d i s p l a y a di stinct

As d e f i n e d here,

p r o j e c t i o n s of the
indentations.

salients

salie nt
de l i m i t

and re entrant
former

ice marg in and r e e n t r a n t s ma r k

These

features are n a m e d

aid discussion.

97

i n f o r m a l l y to

98

Camp 10
surface
Charlevoix
bedrock' " ■3"
valley
T hrough
valleys

—

mv

v

yji.-y.;;:

Surface
A

G rand
T raverse
Bay lowland

APEX

ELMIRA

SALIENT

ABANDONED
FARM REENTRANT

Alba
bedrock
valley

Alba
surface

ALBA

SALIENT
MANCELONA
REENTRANT

Torch Lake
lowland

'.I

V.4

Crofton
surface " Z
KALKASKA
SAUENT

Figure 33. Relationship am ong salients, reentrants,
through valleys, residual terraces, and bedrock valleys.

99
The e x t e n s i v e

Kalkaska

c o n c a v e to the n o r t h w e s t
of the

sa l i e n t

exhibits

that p a r a l l e l s

a broad arc,

the e a s t e r n

b e d r o c k l o w l a n d o c c u p i e d by G ra nd Tr a v e r s e

El k and T o r c h

Lakes

(Fig.

33).

F a r t h e r north,

sm al le r E l m i r a and A l b a s a l i e n ts

align,

and A l b a

Bedrock
elsewhere

(1978),

K o t e f f and Pessl

to t h i c k e r

(1982).

Coincidence

Kote ff

be tw ee n

in the st ud y are a pro ba bl y

ice ov e r v a l l e y s dur in g

advance,

in h i g h e r v e l o c i t y an d g r ea te r outflow.

bases,

some m a j o r l a n d f o r m tre nd s

interpreted

bedrock

Cadwell

and b e d r o c k v a lle ys

resulting

positions

(1976),

and M u l h o l l a n d

are

ice m a r g i n a l

(1960),

(1981),

these

on

by Kaye

Rieck

is due

tre nding

been d o c u m e n t e d

(1974),

sa li en ts

the much

b e d r o c k valleys.

i n f l u e n ce

has

Bay and

respectively,

w i t h the c o m p a r a b l y sized n o r t h w e s t - s o u t h e a s t
Charlevoix

flank

to be

influence.

b e d r o c k lowlands,

in large part

For example,

On

in the st ud y area

the res ul t

salients

of strong

a l ig n with

r e e n t r a n t s w i t h b e d r o c k highs.

L a n d f o r m s a s s o c i a t e d w i t h the
I nne r Port H u r o n C o m p l e x
To
Complex

f a c i l i t a t e di sc ussion,
is d i v i d e d into

2) distal

1982).

i n t e r p r e t e d below.

and Taylor,

zone,

and

(Ma nc el on a Plain).

th ese h u m m o c k y p r o x i m a l

(L ev ere tt

and Bell,

Inner Port H u r o n

1) a p r o x i m a l h u m m o c k y

t e r r a c e d o u t w a s h p l ai ns

Prev iou sly ,
mo ra i n e

the

1915;

zones we re
Martin,

map pe d as

1955;

Bot h areas are d e s c r i b e d and

Farrand

100

PRO X IM AL TRA CT S
The crest

of the Inner Port H u r o n C o m p l e x tren ds

northeast-southwest

for about

from 315 m in the so ut hwe st
int er lo ba t e
d is t in c t

tract.

In c r o s s - s e c t i o n the

range

feature has a

w i t h a steep no rt h w e s t -

slope and a gen tl e dis ta l d e c l i v i t y

13).

R e l i e f on the

Hill,

w he re the Jor da n River

slope,

Altitudes

to 450 m at the apex of the

a s y m m e t r i c al profile,

facing p r o x im a l

Numerous

60 km.

former e x ce ed s

(Fig.

130 m at D e a d m a n ’s

is at the base of the bluff.

ice b l o c k de p r e s s i o n s

are a s s o c i a t e d w i t h the

and at m a n y loca ti on s b o u l d e r s are c o n c e n t r a t e d

al on g the crest.
In many places,

the gentle di st a l

h u m m o c k y t o p o g r a p h y nearest
i n t e rl ob at e ap e x this zone

the crest.

slope di sp l a y s
At the

is 4 km wide and co nt ai ns

numerous

clo se d d e p r e s s i o n s

and p e r f o r a t i o n

Pro f i l e s

show that the highe st

features.

su rf a c e s m a r k the

remnants

of an o u t w a s h p l a i n that c o r r e l a t e s w i t h the E l m i r a
Plain.
Southward,

the h u m m o c k y zone na r r o w s to a w i d t h of

one k i l o m e t e r near the O t s e g o - C h a r l e v o i x C o u n t y line.
N o r t h w e s t of Mancelona,

it w i d e n s a g a i n and co nt a i n s

b lo ck d e p r e s s i o n s up to 20-30 m deep.
corresponds
thus,

w h e r e the p l a i n

32)

W i d t h of this area

to the full b r e a d t h of the M a n c e l o n a Plain -is wide,

A l t e r n a t i n g areas of co ll ap se
(Fig.

ice-

are

so is the h u m m o c k y zone.
and n o n - c o l l a p s e

found farther south.

H i g h rel ie f

topography
(38-44 m),

101
u n c o n t o l l e d d i s i n t e g r a t i o n fe at u r es are e s p e c i a l l y
well d e v e l o p e d n e a r M a y v i l l e Lake
T.

29 N . , R.

(SW1/4,

SW1/4,

sec 26,

7 W . ).

Dry h an gi ng v a l l e y s
and 1 km long,

(Fig.

2),

are c o n c e n t r a t e d

some n e a r l y

15 m deep

in three areas:

1) at the

Inner Port H u r o n apex,

2) b e t w e e n Al b a and Elmira,

no r t h w e s t of M a n c e l o n a

(Fig.

south of M an ce lo na .
of the declivity,

32).

None are

identi fi ed

Some hang n e a r l y 75 m above the base

ma n y of the ch an n e l s c o n t a i n kettles,

and all exte nd p e r p e n d i c u l a r to the trend of the
co nt ac t
modern

slope.

Their

stream,

i mp re ss iv e

size,

ice-

lack of a

and ab s e n c e of a h e a d w a t e r area indicate

fo r ma ti on by m e l t w a t e r streams
margin.

and 3)

Furth er mo re ,

d e v e l o p e d at the

flowing off the

ice

they are d e ep es t and best

steep pr ox i m a l

slope,

i nd ica ti ng

that

the u p s t r e a m p o r t i o n of the v a l l e y must have been
su p e r g l a c i a l

or englacial.

fi llings or o t h e r e v i d e n c e
associated with

No

feeding e s k e r s , cre vasse

for su bg l a c i a l

the pr oximal

dra in ag e

are

slope where the hangi ng

va l l e y s are found.
In places,

small

al luvial

fans,

co ve r i n g about a

q u a r t e r sur ve y section,

e x t e n d s o u th ea st

Inner Port H u r o n crest,

add in g

relief to the

These

feature.

from the

an a d d i t i o n a l

10-15 m

la n d f o r m s have asymme tr ic

fan-like p r o f i l e s

and are best d i s p l a y e d at D e a d m a n ’s

Hill

28,

(SW1/4,

sec.

ju nc t i o n of M-32
N.,

R.

5

W . ) and

T.

31 N.,

an d US-131

R.

(SE1/4,

in the SE1/4,

5 W.),

near the

NE1/4,

SW1/4,

sec.

sec.

15,

5, T.

T.

31

28 N.,

102

R.

7 W.

(Fig.

32).

in M ic hi g an are
large

Si mil ar l a n d f o r m s

i n t e r p r e t ed as

sup erg la ci al

above the general
(Rieck,

1976;

N u me ro us

sites where es pe c i a l l y

stream s d e p o s i t e d sand and gravel
san du r level du ri n g

Bl ewe tt and Rieck,

is ap pr opr iat e

from ot her studies

for small

linear

1987).

al l u v i a l

ridges are

final de g l a c i a t i o n

fans

This e x p l a n a t i o n
in the stu dy area.

i d ent if ied pr ox i m al

to the

steep Inner Port H u r o n slope n o r t h and west of Mancelona.
They are

.5-1

km in length,

the Inner Port Hu ro n bluff,
stra tif ed drift.

o r i e n t e d p e r p e n d i c u l a r to

and com po se d

The ir mo rp ho log y,

of ice -contact

composition,

and

close a s s o c i a t i o n wi t h the Inner Port H u r o n pro xim al
slope

indicate

stagnant

ice.

among others,

fo rm at io n as d i s i n t e g r a t i o n ridges
Si mi la r
Flint

la nd fo rm s

(1928),

in

have bee n de s c r i b e d by,

Pr ice

(1973),

and R ie ck

(1976).

CONCLUSIONS
On the basis of
profiles,

i) a s y m m e t r i c

2) bou ld er s along

3 ) evi de nc e

for ice -co nta ct

the

perched

s t r a t i f e d drift

fans,

contact

including dry

the steep pr o x i m a l

Inner Port H u r o n C o m p l e x
slope.

la nd fo rm s

from Chapte r

ice block dep ressions,

feeding d i s i n t e g r a t i o n ridges,
of the

fan-like

Inner Port H u r o n crest,

2, and 4) pre se nc e of s t a g n a t i o n
hangin g valleys,

all uv ia l

and

slope

is i n te rp re te d as an ice-

A s s o c i a t e d h u m m o c k y t o p o g r a p h y eve nt ua ll y

formed along the crest of the

Inner Port H u r o n Comple x

from me lti ng of ice blocks c o v e r e d

by dr ift duri ng

103

de gl aciation.

This

are not mo ra i n i c
Taylor,

1915;

indicates that pr oximal

as mapped by oth er s

Martin,

1955;

Riec k

(Le ve r e tt and

F a rra nd and Bell,

inste ad ma r k t e r r a i n formed along
de s c r i b e d by Ko t e f f

regions here

and Pessl

1982),

but

a head of o ut wa sh as

(1981),

and Blewe tt and

(1987).

F LU VIA L AND G L A C I O F L U V I A L SU RFACES OF THE
MA N C E L O N A PLAIN
Le ve r et t and Taylor
Plain"

(1915)

appli ed

to the v a l l e y train se pa r a t i n g their

Port H u r o n moraines.

Becau se

not one,

10 dis ti nc t

but at least

"Ma nc el on a Plain"
wh ol e

the term

the presen t

"Mancelona

Inner and Outer

study recognizes

surfaces here,

the term

is used only w h e n refe rr ing to the

of this area.

Since these

d o c u m e n t e d previously,

surfaces have not been

they are de s c r i b e d

in detail

below.
Th ree

extensive,

hig he r surfaces,

and seven

smaller,

lower terraces are rec og ni ze d bas ed on detaile d

an aly sis

of 7 1 / 2 ’ top ogr aph ic maps

contours),

field observation,

dr aw n at right
34).

and to p o g r a p h i c pr of i l es

angles to as su me d

The ma i n surface,

(3 and 5 m

co ve rin g

flow di r e c t i o n

(Fig.

75% of the M a n ce lo na

Plain,

is inf or ma ll y named the Elmi ra Pl ai n

Excep t

for the Cr of to n terrace and H o f f m a n Lake Channels,

w h i c h are tr ea t e d separately,
Elm ir a Plain)
to lowest

all

surfaces

are numbere d se q u e n t i a l l y

(#8).

(Fig.

32).

(including the

from highes t

(#1)

CROFTON
SURFACE

CAMP TEN
SURFACE (1)

ALBA
SURFACE

— 400m—
612
SURFACE

ELMIRA
SURFACE (2)

612

345
>330

— **

7 **
■300
7 ».270

RAPID RIVER

RUGG POND
miles

Figure 3 4 . Principal su rfa ces of the M ancelona Plain

NE

104

CLOSE-UP SHOWING SURFACES 3-8
SW

105

Crofton

surfa ce

-- The C r o f t o n o u t w a s h surface,

immediately proximal
K a l k a s k a County,

to the O u t e r Port H u r o n C o m p l e x

is the u p p e r m o s t t e r r a c e

the M a n c e l o n a Plain.
m / k m and e x h i b i t s

scarp c o n t a i n s
depre ss io ns ,
meltwater
feature
that

erosion.

Altitude

to surface

this a r e a was

to be d e g l a c i a t e d

the

(Camp Ten,

c o r r e l a t e d on
Overall

approximately

1 (see next

Alba,

and

612

for

20%

isos ta ti c

(L everett and Taylor,
1.5 m/km,

and the

alignment

is l o c a t e d

here

large s a l i e n t s

da t a a s s o c i a t e d w i t h

instea d of

in C h a p t e r 2.

(Fig.

34).
since

is

(Fig.

w i t h the

34).

Each

i m m e d i a t e l y pr o x i m a l
hol d e x t e n s i v e

ones h a r b o r sm al le r s u r f a c e s
To

and

surface m e r g e s

r e m n a nt s

b r i e f l y below.

implies

separate

rebound

1915),

of the

sed ime nt

section),

surfaces),

2) ne a r K a l k a s k a

described

the C r of to n

4).

(surface

small

ice b lo ck

1 is r e p r e s e n t e d by three

adjusted

a m a j o r salient;

or

pa r t of the M a n c e l o n a Plain

E l m i r a Pl ai n
three

st eep pr ox i m al

be e n t r i m m e d by s u b s e q u e n t

the basis of p r o f i l e

slope,

deglaciation

Its

and p o s i t i o n of

first

(see Ch.

1. -- Su rf ac e

te rr a c e s

it has

1.2

b r o k e n by o c c a s s i o n al

low sand dunes.

suggesting

in

r e c o g n i z e d on

s o u t h w e s t w a r d at

no b o u l d e r c o n c e n t r a t i o n s

re la t i ve

Su r f a c e

It sl o p e s

flat t o p o gr ap hy,

sh a l l o w k e t t l e s and

locat ed

(Fig.

33).

to

terraces,
All

are

s i m p l i f y di sc us sio n,
each te r r a ce

are pr o v i d e d

106
CAMP TEN SURFACE:
(Fig.

33),

this

Locate d proxima l

ge nt l y rolli ng

the E l m i r a Plain,

tract

incr ea se d relief.

indica ti ve of b r ai d e d me l t w at er

g l a c i o f l uv ia l

Faint
streams,

and v e r i f y a

o r i g i n for the deposits.

Like the E l m i r a Plain,
some cla st s e x c e e d i n g
the edge of p o t a t o

14 cm

fields.

numerous

stone piles,

in b-diameter,

are

A v e r a g e b-d ia me te r

from four sampled piles

was 7.8 cm.

scarp

ice blocks and

are i d e n t i f ie d on aerial p h o t o g r a p h s

stones

25 - 30 m above

or boulder

Melti ng of buried

po st g l a c i a l d i s s e c t i o n have
scroll marks,

lies

and di sp l a y s a steep pr ox ima l

devo id of ice bl ock de p re ss io ns
co nce ntr ati on s.

to the E l m i r a salient

(50 stones

No s i g n if ic an t p a t t e r n

with

locat ed at
of 200

from each pile)

in average b-

diameter

is o b s e r v a b l e among stone piles ac ro s s

surface,

but s e d im en ts overall

the

are mu c h co ar se r than Alba

and 612 deposits.
AL B A SURFACE:

The A l b a terra ce

is more d i s s e c t e d than the

Camp Ten s u rf ac e and li e s 12 - 15 m above the E l mi ra
Plain.

Its st ee p pr oximal

concentrations

or

s ca rp lacks b o ul de r

ice b lo ck depressions.

pit at the base of the pr ox im al
sec.

29,

clay,

T.

30 N.,

but surf ic ia l

fine gravel,

R.

slope

A small gravel

(NE 1/4,

NE 1/4,

5 W . ) co nt a i n s brown la cu st ri ne

terrace de po s i t s consi st of sand and

w i t h a few clasts ap p ro ac hi ng

5 cm in b-

diameter.
A second,
Elm i r a Plain,

h i g h e r surface,

lying

18-21 m above the

b ar e l y cov er s a q u a r t e r survey section,

and

107

is locate d on the n o r t h we st

fl ank of the ma i n Alba

surface

of its small

(Fig.

32).

Be ca us e

u n c e r t a i n significance,
of surface

1 that

612 SURFACE:
exhibit s

This extensive,

a straight pro xi m a l

33).

this

(surface

d i s s e c t i o n by h ea dw at er s
the relief.
amounts of

Se di men ts

2,

m o d e r a t e l y kettle d plain,
scarp w h i c h

is align ed with

te rra ce
Fig.

g r a d u a l l y merges with

34).

Ho lo c e n e

of the Rap id Ri ver has

are p r i m a r i l y

increased

sand w i t h limit ed

fine gravel.

M o r p h o l o g y and s ed im en ts
te rra ces

in dis cus sio ns

s lope of the M a n c e l o n a reentrant

Southward,

the E l mi ra Plain

inc lud ed

follow.

the n o r t h w e s t - f a c i n g
(Fig.

it is not

size and

in di cat e that

these three

are rem nan ts of a single ou tw a s h surface that

was once more extensive.

E v i d e n ce

includes:

1. Te rr ac e el ev a t i o n s bec om e p r o g r e s s i v e l y lower
s o u th wa rd (Fig. 34), p r o d u c i n g a smoo th con caveu p w a r d profil e t yp ic al of o u t w a s h surfaces.
2. Ter ra ce s lack ice b l o c k d e p r e s s i o n s along proximal
scarps, su gge sti ng that these slopes are erosional,
rat he r than ic e- co nta ct slopes.
3. Te rra ce scarps are a l i g n e d w i t h t r u n c a t e d
ree nt ra nt s of the O u t e r Port H u r o n C o m p l e x (Fig. 33),
in dic ati ng that scarps form ed by m e l t w a t e r trimming,
rat he r than ice -c on ta ct deposition.
4. T e rr ac es lack p r o x i m a l b o u l d e r concentrat ion s,
in dicating that pro xi ma l areas may not represent ice
m a rg in al positions.
5. Some terrace scarps ex hi bi t a bo ul d e r lag proximal
to the base of the slop es (Fig. 15), po s s i b l y
in dic ati ve of m e l t w a t e r tri mm in g (see Ch. 4).

6. S ed ime nt s bec om e p r o g r e s s i v e l y finer southward,
b a s e d on vi s u a l reconnaissance, s ug ge st in g that these
sur f a ce s ma y m a r k re mn ant s of an i n teg ra ted
g l a c i o f l u v i a l system.
7. P os i t i o n i n g of terraces w i t h i n p r o t e c t e d salients
s u g g e s t s that these su rf ac es we r e once more
extensive.
Ev e n a slight e x p a n s i o n of these surfaces
t o w a r d the n o r t h w e s t wo ul d u n i t e the re mn a n t s in a
single surface.
O n all these bases,
terraces
surface

the Ca m p Ten,

are i n t e r p r e t e d as r e m n a n t s

Alba,

of a single o u twa sh

that was once more e x t e n s i v e

(surface

s u p e r f i c i a l l y r e s e m b l i n g kame terraces,
su rf a c e s

exhib it m o r p h o l o g y typic al

and p r o b a b l y re p r e s e n t ve st i g e s
gl a c i o f l u v i a l

1).

Tho ug h

the three

of o u t w a s h surfaces,

of an in te g r a t e d

s y s t e m that d r a i n e d s o u t h w e s t w a r d .

E l m i r a surface —
widens

and 612

The E l m i r a s u r f a c e

from 2 to 11

s o u t h w e s t w a r d at

is 75 km long,

km toward the south,

1.2 m/km.

This

slope

and slopes

is a d j u s t e d

for

iso st at ic

rebou nd of a p p r o x i m a t e l y

estimates

of isos ta ti c r e bo un d fr o m L e v e r e t t and Tayl or

(1915),

20% b as ed on 1 )

and 2) an an al ys is of d i f f e r e n t i a l u p l i f t of

ab a n d o n e d

shorelines

study area)

across

(located

i m m e d i a t l e y we s t of the

lat it ud es c o r r e s p o n d i n g to n o r t h e r n

and s o u t h e r n b o u n d a r i e s of the s t u d y area.
s o u t h e r n segments exhib it a d j u s t e d
and 1.0 m/km,

respectively

subtle c o n c a v e - u p w a r d
sand ar
(Fig.

(Fig.
36)

35;

(Fig.

Church,

1972).

slopes of 1.5 m / k m

34),

longitudinal

producing

the

p r o f i l e t y p i c a l of

This low r e l i e f pl ai n

is p u n c u t u a t e d by s c a t t e r e d

depressions

N o r t h e r n and

(with co nc en t r a t i o ns ),

ice b l o c k

e r o si on al d r y channels

LEWIS SANDUR
(CHURCH, 1972)
Length: 1 km

TINGIN SANDUR
Length: 5 km
V.E.: 20

WHITE RIVER SANDUR
(FAHNESTOCK, 1953)
Length: 2 km
V.E.: 2

HOFFELLSSANDUR
SUNDBORG, 1954)
Length: 15 km
V.E.: 20

SLIMS RIVER (RUST. 1978)
Length: 26 km
V.E.:21
ELMIRA SANDUR
(THIS STUDY)
Length: 75 km
V.E.: 20

Figure 35. Profiles of s e le c te d sandar.

110

Figure 36. View southeastward across the Elmira Plain
near Alba; the proximal slope of the Outer Port Huron
Complex is in the distance.

Ill
in pr ox i m a l areas nor th of Mancelona,

and,

southward,

scatt er ed d u n e s .

P R I N C I P A L L A N D F O R MS OF THE E L M I R A SURFACE:
Kettle chains

- Th re e kettle

chains trend no rt hw e s t -

southeast ac r o s s the E l m i r a surfa ce n o r t h w e s t of Elmira
(Fig.

32).

These

chains are more than 3 km long,

some d e p r e s s i o n s ex c e e d i n g
de cr e a s i n g

30 m in depth,

with

and d i s p l a y

kettle bo t t o m a l t i t u d e s no rt hwe st wa rd .

The

eas t e r n m o s t c ha in aligns w i t h the trend of the th r o u g h
yalley containing
Near Wetzel,

the Boyne R i v e r ’s South Branch.
a northwest-southeast

chain c o n t a i n i n g S a t t e r l y Lake
R.

6 W . ; Fig.

Likewise,

32),

(SW1/4,

to valle ys

(Fig.

1979;

30 N.,

B le we tt and Rieck,

surfa ce
1987).

duri ng d e g l a c i a t i o n

Lake

32).

in M i c h i g a n are

in the p r e - l a s t ad v a n c e

interpretation,

re lat ed

(Rieck and
In this

sta gna nt

ice lingers

in v a l l e y s and ma y be c o v e r e d by o u t w a s h

sediments.

G r a d u a l m e lti ng

linear k e tt le s
lowland.

T.

a n e a r b y kettle ch ai n c o n t a i n i n g W e t z e l

Si mi la r fe atures e l s e w h e r e

longest

sec 26,

kettle

is a l i g n e d w i t h C a s c a d e C r e e k Gorge.

aligns w i t h the G r e e n R iv er V a l l e y

Winters,

or i e n t e d

of this

that mark the course

Alignment

of ke t t l e cha in s

ice forms a series of
of the p r e - e x i s t i n g
on the E l m i r a

surface wi t h th r o u g h v a l l e y axes to the n o r t h w e s t
strong e v i d e n c e

for c o in c i d e n c e of b e d r o c k lows

kettle chains.

O n these bases,

sections of the E l m i r a P l a i n are

ket tl e ch ai n s

is

and

in no rt her n

i n te rpr ete d as

features

112
likely marking

the co u r s e of p r e - e x i s t i n g

In ci s e d va l l ey s

-

Numerous

small

lowlands.

in ci se d v a l l e y s

are

i d e n t i f i e d on the E l m i r a P l a i n n o r t h of Mancelona.
b e g i n at the I nne r Port H u r o n i c e - c o n t a c t
hanging valleys
perpendicular
Plain

(Fig.

a n d t re nd s o u t h e a s t w a r d

to the

34).

former

l i k e l y are g r a d e d to t e r r a c e s
su rf a ce

(3-8).

fe at u r es

Maizels

acro ss

5 m deep,

(1983b)

i nt er pr et s

i n te r p r e t e d

s i mi la r

surfaces.

in c i s e d va ll ey s

E l m i r a P l a i n as su r f a c e s m a r k i n g
abandonment

and

l ow er th an the E l m i r a

the t r a n s i t i o n to low er e q u i l i b r i u m
st ud y

the Elm ir a

1 km long,

as n o n - e q u i l i b r i u m m e l t w a t e r ch an n e l s

the pr es e n t

as

(i.e.

ice margi n)

T h e y av era ge

slope

Most

ma r k i n g
Likewise,

on the

the t r a n s i t i o n

from

of the E l m i r a P l a i n to e s t a b l i s h m e n t of lower

o u t w a s h terraces.

Terraces

3-8 -- B a s e d on t o p o g r a p h i c

terraces

l ow er t h a n the E l m i r a

within a narrow
Rapid River

zone

(Fig.

ice.

34).

The

s u r f a c e are

six
identified

c e n t e r e d on the h e a d w a t e r s
Surfaces

k e t t l e s and l i k e l y for me d
stagnating

data,

3,

4,

5, and 8 c o n t a i n

in a s s o c i a t i o n w i t h

first t h r e e s u rf ac es c o m p r i s e a

s t e p p e d seri es of p r o g r e s s i v e l y l o w e r terraces,
curvilinear

sca rp s c o n c a v e to the n o r t h w e s t

D o w n s t r e a m e x t e n s i o n s of t e r r a c e s
by s t a g n a t i o n t o p o g r a p h y we s t
burial

in cludes

relatively

of the

3,

4,

e a c h with

(Fig.

32).

and 5 are bu ri e d

of Kalkaska.

Evidence

for

1) an a b r u p t d o w n s t r e a m t e r m i n a t i o n of

smooth outwash surfaces

by u n c o n t r o l l e d

113
d i s i n t e g r a t i o n topography,

and 2) a l t it ud es w i t h i n these

d i s i n t e g r a t i o n tracts that are m u c h too high to corr el ate
w i t h su rfaces
Burgis

3, 4,

(1977)

and 5.

i n t e r p r e t ed n e a r l y

a s s o c i a t e d wi t h the Au Sable R i v e r
M i c h i g a n as features m a r k i n g

include

from wide,

to single chann el

streams c o n t r o l l e d by p r e c i p i t a t i o n and

groundwater.
3-8

la ndforms

in n o r t h e a s t e r n

the t r a n s i t i o n

m u l t i p l e - c h a n n e l m e l t w a t e r s t re am s
po s t - g l a c i a l

id entical

Ev id e nc e

for s i m i l a r ge nes is of ter rac es

1) n ar ro win g and

s u c c e s s i v e l y lower surfaces,

in c r e a s e d

s i n u o s i t y of

an d 2) m o r p h o l o g i c

si m il ar i t ie s be tw ee n low al t i t u d e

te rraces

and 8) and the m o d e r n R ap id R i v e r Valley.

(surfaces

7

Significance

«

of these

la ndforms

is d i s c u s s e d

H o f f m a n Lake C h an ne l

—

Eight h a n g i n g v a l l e y s a l o n g the

Inner Port Hu ro n apex co nv e r g e
H o f f m a n Lake Chann el
km wide,

8 km long,

con t a i ns nu mer ou s

(Fig.
slopes

shallow,

southeastward

32),

of H ear t Lake,

This chann el

2)

.5- 1.2

and
lakes.

h i g h e r than the m a i n

i d e n t i f i e d at 365-370 m south

indica ti ng

large size,

Lake.

su rfa ce c o nt ai ns

drainage

southward.

1) pr es e n c e of dry h a n g i n g va lle ys at

depressions

is

d r y k e tt le s and k e t t l e

in the h i g h e s t

im br i c a te d gravels

u p s t r e a m end,

form the

and at 360-365 m n o r t h of H o f f m a n

small gravel pit

The

are

to

so ut h and eastward,

Two p o o r l y d e v e l o p e d terraces,
H o f f m a n Lake Channel,

in Ch ap t e r 4.

its

3) p r e s e n c e of ice b lo ck

in the channel bottom,

and 4) e v i d e n c e

for

A

114
drainage
feature

s o u t h and east,

in dicates

that the H o f f m a n Lake

is a former m e l t w a t e r channel,

w h i c h d r a i n e d an

ice m a r g i n s i t u a te d along the n o r t h w e s t

flank of

the

Inn er Port H u r o n apex.

S u m m a r y -- The e x t en si ve nat ur e of sur fac es
ind icates

that

they are e q u i l i b r i u m surfaces,

r e l a t e d to q u a s i - s t a b l e
1978;

Maizel,

s ur fac e

1983b).

ice m a r g i n a l p o s it io ns
Ket tl e

rep res ent the t r a n s i t i o n

to lower terraces.

Ter ra ces

(Ritter,

chai ns a s s o c i a t e d with

and their distal e x te n s i o n s

incise d valleys)

2

possibly

2 like ly mark the tr end of p r e - e x i s t i n g

H a n g i n g va l l e y s

cha n g e

1 and

3-8 most

lowlands.

(small

from surface

2

li ke l y re c or d the

from m e l t w a t e r - d o m i n a t e d p r o g l a c i a l

braided

streams to p r e c i p i t a t i o n / g r o u n d w a t e r c o n t r o l l e d n o n ­
glacial

stream s c h a r a c t e r i z e d by a single channel.

H o f f m a n Lake c h an ne l

The

r e pre se nts ea s t w a r d d r a i n a g e

in it ia te d som et im e a ft er a b a n d o n m e n t of the E l m i r a
surface.

I n t e r p r e t a t i o n and s i g n i f i ca nc e

su rf ac es duri ng

final d e g l a c i a t i o n

of these

is d i s c u s s e d

in

C h a p t e r 4.

Post

Land for ms of the
Inner Port H u r o n zone

A l t h o u g h this tract does not ex h i b i t
ide nti fi ab le

ice mar gi na l

ha ng in g valleys,
the

heads of outwash,

and pro ximal

for the

p e r c h e d fans,

b o ul d e r c o n c e n t r a t i o n s

Inner and Ou te r Port H u r o n Complexes,

position

easily

ice m a rg i n can be

like

an a p p r o x im at e

inf erred on the basis

115
of o u t w a s h te rr a c e s

i nc ise d

ic e- c o n t a c t

The a r e a ’s n o r t h w e s t e r n b o u n d a r y is

marked

slope.

into

the

Inner Port H u r o n

in most p l a c e s by a s h a r p m o r p h o l o g i c c o n t r a s t

between glaciofluvial terraces
Inner Port H u r o n
Most o u t w a s h
the Jordan,

separate

flut ed uplands.

s u r f a c e s are a s s o c i a t e d w i t h v a l l e y s of

Green,

All un derfit,
ancient

zone and the

b e l o n g i n g to the Post

these

and C e d a r
strea ms

i ng ro wn m e a n d e r s

riv er s

and W a r n e r Creek.

o c c u p y the b o t t o m s

up to

of large,

1.6 km in a m p l i t u d e

37).

P a l e o d i s c h a r g e s b a s e d on m e a n d e r w a v e l e n g t h

1965)

in the J o r d a n V a l l e y are

33,600

ft3 sec', c o m p a r a b l e

at Sidney,

to the m o d e r n Y e l l o w s t o n e

to v a l l e y trend,

c o m p l i c a t e d a r r a y of small,
38).

a lt it ud e

transitional

twe lv e t e r r ac e s

terraces,

associated with

Y,

Z,

E,

re sp ec ti vel y.

ice m a r g i n a l

to the s i g n i f i c a n c e
te rr ac es

River

of pr of i l e s

su rf ace s

into three types:

terrace,

C e d a r - G r e e n river valleys:

verifiable

to

and fo r m a

i s o l a t e d re si d u a l

T h e y c a n be d i v i d e d
high-altitude

and W, X,

17,800

here are c o r r e l a t e d on the basis

d r a w n at right a n g l e s

e x t e n si ve

(Dury,

Montana.

Terraces

(Fig.

approximately

(Fig.

A;
B,

1) an

2) three m e d i u m C,

and D;

a n d 3)

the J o r d a n - W a r n e r and

El,

F,

FG,

G,

G H 1 , G H 2 , H,

W i t h the g e n e r a l

lack of

p o s i t i o n s here and u n c e r t a i n t y as

of G r e a t l a k e a n / V a l d e r a n events,

are d e s c r i b e d o n l y briefly.

these

116

Figure 37. View from the Deadm an’s Hill overlook
of the underfit Jordan River with large paleom eanders.

NE

SW
CEDAR-GREEN VALLEY

400

JORDAN-WARNER VALLEY

Z COMPLEX
\v

300

W arner CreekJo rd an River

G reen,
C edar River

River
GH2
200

Orri

10ml

20mi

F g u re 3 8 . Principal glaciofluvial/fluvial su r fa c e s
of th e C edar-G reen and Jordan-W arner v alleys.

30 mi

METERS

D?
S urfaces associated
with the Lake of th e
W oods Plain

118
SURFACE A
This

flat,

s o u t hw es t

a d j u s t e d slope)

c o n t a i ns

d e p r e s s i o n s or c r e s t a l
and

is best o b s e r v e d

US-131,
Road,

and 2)
At

the

w i t h the A l b a
and

shows

sloping

su rf ac e

no p r o x i m a l

boulders

ice blo ck

like

the E l m i r a

1) on h i g h w a y M-32,

la tt e r

location,

s al ien t of the

the

s u rfa ce

ou t w a sh

su r f a c e s

the base of the

S u r f a c e B is

transition
(A and B)

B,

in the ce n t e r of

i d e n t i f i e d along

ice-contact

C,

incised 20-25

Inner

S o u t h w e s t w a r d , scattered

Inner Port H u r o n

SUR F A C E S

exist

in bo t h the

t e r r a c e s c o r r e l a t i v e w i t h S u r f a c e A are

32).

is a ss oc ia te d

I n n e r Port H u r o n Complex,

and O u t e r Port H u r o n C om pl ex es .

(Fig.

km west of

s im i l a r l a n d f o r m r e l a t i o n s h i p s

b e t w e e n s a l i e n t s and

W.

0.5

Plain,

i m m e d i a t e l y n o r t h of A l b a on J o r d a n River

that

best o b s e r v e d

(1.2 m / k m

slope.

and D

m b e l o w surfa ce A,

and is

sec.

R.

10,

T.

31 N.,

5

S u r f a c e s C a n d D a p p a r e n t l y m a r k the

from higher,
to lower,

mo r e

s m al le r

extensive outwash
fluvial

C e d a r and J o r d a n R i v e r v a l l e y s

terrac es

(Fig.

surfaces

in the

38).

S U R F A C E S O F THE C E D A R - G R E E N R I V E R V A L L E Y
Here,

t e r r a c e s W,

w i t h a lower t e r r a c e
relationships
co n t a c t

X,

(Fig.

assemblage

are unclear.

All

38)

240-2 50 m,

with

the o t h e r a b o u t

may correlate

(Z complex),
are

but

gr a d e d to an ice-

l a c u s t r i n e p l a i n or kame d e l t a

Lake of the W o o d s Plain),
at

and Y

(i n f o r m a l l y named

two d i s t i n c t
2 5 0-2 55

m

surfaces,

(Figs.

32,

one

38).

119

The

Lake of the Woo ds

pr o g l a c i a l

featu re p r o b a b l y

Fig.

32).

is n o w o c c u p i e d by Lake

Associated

ice -c on ta ct

characteristics

include

w e s t e r n margin,

and 2) p r e s e n c e

proximal

su gg e s t i n g mass wa st i n g

scarp,

m a r g i n a l l y st agnant
sho re l in es
v a ll e y

in a

lake at the s o u t he rn end of a th ro ug h vall ey

(the lowest part of w h i c h
Bellaire;

formed

1) n u m e r o u s

ice.

lake was c o n f i ne d

of a rim along

In addition,

or l acu str in e

farther north,

kettl es along

remnan ts are

i nd ica ti ng

the

of sedim ent s

from

no c o rr es p o n d i n g
id en ti fi ed

in the

that the p r og la c i a l

to the s o u t he rn

that tne re m a in de r c o n t a i n e d

its

part of the v a l l e y

and

ice.

SU RF A CE S OF THE JO R DA N R I V E R - W A R N E R C R E E K V A L L E Y
Eight

surfaces are r e co g n i z e d w i t h i n the Jor da n River

V a l l e y and are d e s i g n a t e d E,
and H

(Fig.

38).

Su rf ace s E,

to a l a c u s t ri ne plain,
Plain,

G.

s u rf ac e G oc cu p i e s

th r o u g h valley,
ev id e n c e of
in w h i c h

El,

but

El,

Like

F,

the

a p p a r e n t l y was c o n f i n e d

formation

to the

be ca us e

sho re l i n es

nor

l acu str in e

the v a l l e y

farth er north.

G-Hl, G-H2,

and G m a y be graded
Lake of the Woods

the s o u t h e r n end of a m a j o r

s e d ime nt s a c c u m u l a t e d

to

and oth er

are absent.

The lake

form surface

G

s o u t h e r n m o s t p o r t i o n of

ne it he r c o r r e s p o n d i n g

te rr ac es
Su rf a c e s

along w i t h the m o d e r n J o r d a n River,
surface G.

F G , G,

ic e- bl oc k d e p r e s s i o n s

ic e-c ont ac t

the th r o u g h valley,

F,

can be

i d e n ti fi ed

in

G - H l , G - H 2 , and H,
are

incised

into

120

S I G N I F I C A N C E O F POST IN NE R PO R T H U R O N T E R R A C E S
The c o m p l i c a t e d

terrace a s s e m b l a g e s w i t h i n the Post-

Inner Port H u r o n zone are d i f f i c u l t
l an df or m re l a t i o n s h i p s
not po s s i b l e until

alone.

there

to in te rpr et based on

A com pl et e

e x p l a n a t i o n is

is a full and a c c u r a t e

u n d e r s t a n d i n g of G r e a t l a k e a n / V a l d e r a n even ts
In general,

however,

from a single,
(surface A)

these t e r r a c e s

record the

m e l t w a t e r d o m i n a t e d br a i d e d

to twin,

non-glacial

in the area.
transi tio n

sy st e m

single c h an ne l

streams

of the C e d a r - G r e e n and J o r d a n - W a r n e r valleys.
Alt oge the r,

these

surfaces

Ho l o c e n e

transition

at least

in part,

1)

r e c o r d the P l e i s t o c e n e -

in the s t u d y area,

and 2) document,

final Port H u r o n deglaci ati on.

L an dfo rm s a s s o c i a t e d wi t h the
O ut er Port H u r o n Co m p l e x
In cross

section,

the O u t e r Port H u r o n C o m p l e x has

an a s y m m et ri ca l to po g r a p h i c p r o f i l e
pi'ox.ijua± scarp and gen tl y
13),

Mos t p r ox im al

hu m m o c k y zone,

da ta

inc li ne d dist al

(Chapter 2)

ice m a r g i n a l

so ut he rn r e gio ns d i s p l a y l a n d f o r m s

a s s o c i a t e d w i t h a series of s u c c e s s i v e

into

se di men tar y

indicate that n o r t h e r n ar ea s are

whereas

On these bases,

(Fig.

into o u t w a s h plain.

mo rp h o l o g i c p r o f i l e s and

c h a r a c t e r i z e d by a single p r o m i n e n t
position,

slope

te rr ai n e x h i b i t s a 1-2 km wi d e

w h i c h grades d i s t a l l y

As de sc ri be d below,

e x h i b i t i n g a steep

g l ac ia l

the Out er Port H u r o n C o m p l e x

1) a n o r t h e r n pro xim al

region,

terminii.

is divided

2) a n o r t h e r n distal

121

region,

and

3)

s o u t h e r n tracts c o m p o s e d of n u m e r o u s

i s ol at ed h ea ds

of outwash.

Ea c h

is d e s c r i b e d and

i n t e r p r e t e d below.

N O R T H E R N P R O X I M A L REGIONS
To f a c i l i t a t e
are d i v i d e d

into

Fig.
and

associations

D i s i n t e g r a t i o n Ridges

32)

- Th ese

10 m high,

ridges,

are c o n f i n e d

Port H u r o n apex.

so u t h ea st

and north -so ut h,

"Y"

Se d i m e n t s
gr av el

pit;

ice-contact

Ch.

2),

and b e t w e e n ridges.
attributed

fe at ur es

southward

in map view

(Fig.

Gr a v e n o r an d Kups ch

n e a r l y 6 km^

>0.5

m are on

to d e p o s i t i o n of

in s t a g n a n t
T.

ice.

31 N . , R.
fe a t u r e s

intervening
(Fig.

Farm

(1959)

features

(Sec 27,

32).

(Fleming

bo ul der s

ri dg e p a t t e r n c o n t a i n i n g

32).

4 W.)

form a

ic e-block
Rid ge s

are

o r i e n t e d n o r t h w e s t - s o u t h e a s t and east-west.

rid ge s

altitudes

both n o r t h w e s t -

co alesce

and n u m e r o u s

150 m wide,

a r e a s of

controlled disintegration

depressions covering

Sin g l e

1 km long,

sediment within crevasses

- T h e s e large,

T . 31 N . , R . 4 V . ;

s t r a t i f i e d drift

Lake 27 D i s i n t e g r a t i o n Ridg es

generally

10,

Oriented

f o r m a t i o n of s i m i l a r

superglacial

polygonal

(Sec

32).

to pr ox ima l

s h ap ed la n d f or ms

are

(Fig.

some

areas

based on t o p o g r a p h y and

a v e r a gi ng

the O u t e r

fo rm in g

pr ox ima l

se ve n s u b r e g i o n s

salient/reentrant
F le mi ng

discussion,

ca n be

of 425

fo ll o w e d 3 km or more,

ra, and d i s p l a y

(1960).

reach

relief up to 42 m.

p r o b a b l y reco rd c r e v a s s e p a t t e r n s

ice as d e s c r i b e d by K aye

m ay

Such

in st agnant

122

E l m i r a South A p r o n
Here,

(SW1/4,

the t o p o g r a p h y c o n s i s t s

v a l l e y s and a s t e e p
exhibiting
evidence

c r e s t a l boulders.

for an

ice-contact

few k e t t l e s

assemblage
with

are

along a s t a g n a n t

T.

31 N. , R.

of p e r c h e d

Al l

Abandoned Farm Hummocks

Thus,

this

of outwash,
ice,

are absent
landform

unassociated
which

10,

T.

30 N.,

(1960,

372)

p.

differential

of A l b a

attributed

(Figs.

genesis

of

fro m an ice ma s s of u n e v e n t hi ck ne ss .

A l b a S a li en t

28,

T.

30 N . , R.

is c h a r a c t e r i z e d by a c o m p l e x of

features.

chains,

Numerous

Kaye

la nd fo rm s to

and s u b t l e

boulders

for a form er

Scattered exposures

but large d i s i n t e g r a t i o n

are c o n c e n t r a t e d ne a r the

15 a n d 22,

ice m a r g i n a l

show s t r a t i f e d

On th es e bases,

- This area

in ci se d dry channels,

combined with morphology,

gravel.

39).

5 W.)

(Fig.

evidence

near an

S c a t t e r e d out crops

sections

and,

-

sand and gravel

road s e p a r a t i n g
15),

5 W.)

such deposits.

(Secs 27,

s h a l l o w ke tt l e

32,

simila r

d e p o s i t i o n of s u p e r g l a c i a l

ne a r here reveal

formed

R.

U n c o n t r o l l e d d i s i n t e g r a t i o n t o p o g r a p h y exi st s
farm n o r t h e a s t

ice was

margin.
(Sec.

abandoned

bluff

Little buried

am o u n t s of b u r i e d
g la ci al

-

h a ng in g

proximal

h u m m o c k y zones

identified.
a head

fans,

5 W.)

are u n m i s t a k e a b l e

slope.

proximal

represents

significant

36,

(70 - 80 m relief)

p r e s e n t here b e c a u s e
and

sec

T.

30 N . , R.

5 W.

provide

strong

p o s i t i o n here.
sand and co a r s e

landform genesis

is in t e r p r e te d

to be s i mi la r to the A b a n d o n e d F a r m H u m mo ck s,

exc ep t that

123

Figure 39. View of proximal hummocky topography
at the Abandoned Farm site in the Outer Port Huron Complex.

124

the A l b a s al i e n t

experienced

dissection possibly
upon deglaciation
A l b a So uth A o r o n
R.

5 W.)

i n it ia te d by a falling w a t e r table

(de scri bed
(Secs.

- Southw ard ,

4,

so ut he as t
NW1/4,
here

in C h a p t e r 4).

5,

7,

8,

ice-contact

17,

T.

18,

T.

29 N.,

slope w i t h crestal

29 N.,

R.

A northwest-

is locat ed

5 W.

in the

Landform assemblages

are si mi l a r to the E l m i r a S o u t h A p r o n and are

interpreted

in the same manner.

Mancelona Reentrant
W . ) - Here,

(Secs

the p r ox im al

14,

15,

slope

and 22,

because

it has

29 N.,

ice m a rg in al

been t r u n c a t e d by m e l t w a t e r

M a n c e l o n a Plain.
zone ex hib it

T.

R.

6

of the O u te r Po rt Hu ro n

C o m p l e x only a p p r o x i m a t e s a f o r m e r

and

and

sloping d i s t a l plains.

o r i e n t e d h a ng in g v a l l e y

sec.

17,

the O u t e r Port H u r o n C o m p l e x

e x h i b i t s a s t e ep p r o x i m a l
b o u l d e r s and g e n t l y

fu rt h e r a l t e r a t i o n by stre am

Disintegration

ridges

position

st re am s on the

in the pro xim al

a weakly developed north-south orientation

rel ie f a p p r o a c h e s

15 m.

L a n d f o r m g e nes is

is si mil ar to

the A b a n d o n e d F a r m Hummocks.

Summary —

Alt og et he r,

these

s e v e n regions

d i s t i n g u i s h e d on the basis of the

1) natu re

associated proximal

slope

i nf lue nce

ice on to po gra phy ,

of b u r i e d

c o n t r o l l e d vs.

( i c e - co nt ac t vs.

u n c o n t r o l l e d to po gra phy ,

post-glacial

di ss ec tio n,

reentrants.

Characteristics

Ta bl e

6.

and

5)

are
of the
eroded),

2)

3) p r e s e n c e of
4) a m o u n t of

r e la ti on to sa l i e n t s and

of ea c h are p r e s e n t e d

in

125

TABLE 6. CHARACTERISTICS OF PROXIMAL SUBDIVISIONS
OF THE OUTER PORT HURON COMPLEX.
Area

Type of
proximal
slope

Influence
of buried
ice

Type of
disinte­
gration

Fleming
Disint.
Ridges

icecontact

significant

controlled

not
significant

reentrant

Lake 27
Disint:.
Ridges

erosional

significant

controlled

not
significant

salient

Elmira
South
Apron

icecontact

not
significant

(not
present)

not
significant

southeast
side of
salient

Abandon erosional
Farm
Hummocks

significant

weakly
controlled
to uncon­
trolled

not
signif icant

reentrant

Alba
Salient

mostl7
erosional

significant

weakly
controlled
to uncon­
trolled

significant

salient

Alba
South
Apron

icecontact

not
Significant

(not
present)

not
significant

southeast
side of
salient.

significant

uncontrol­
led to
weakly
controlled

significant
along
margin

reentrant

Mance­
erosional
lona
Reentrant

Amount of
post glacial
dissection

Salient or
reentrant
location

126

W i t h m i n o r exceptions,
A l b a So ut h apro ns
Elsewhere
the

ex hib it

o n l y the El m i r a So ut h and

a true

i c e- con tac t

slope.

along the O u t e r Port H u r o n pr ox i m a l

1) a l i g n m e n t of terrac e

scar ps

w i t h the O ut er Port H u r o n bluff,

on the M a n c e l o n a Plain

2) pr es e n c e

of a boulder

lag just west of the O u t e r Port H u r o n slope,
curvilinear
acclivity,

form

(concave to the west)

and 4)

H u r o n crest,

all

lack of b o u l d e r s
indic ate

ac c l i v i t y

3)

smooth,

to parts

of this

along the O ut er Port

that the

slope has been altered

by sub se qu en t m e l t w a t e r erosion.
Int erestingly,

the simila r E l m i r a So uth and Al ba

S o u t h la n d f o r m a ss e m b l a g e s are
l o c a t i o n rel ative

lo c a t ed

to their r e s p e c t i v e

for this are unclear.

Re e n t r a n t

in the same
salients;

reasons

regions d i s p l a y strongly

l i n e a t e d c o n t r o l l e d d i s i n t e g r a t i o n t o p o g r a p h y east of
E l m i r a and muc h we ak e r a l i gn me nt

southward.

The A l b a and

E l m i r a salient s g e n e r a l l y c o n t a i n large r d i s i n t e g r a t i o n
ridge s

and gr ea t e r p o s t - g l a c i a l

reentrants.
r u gg ed

Th es e

region s also

t o p o g r a p h y b e cau se

w h i c h we re pr e f e r r e d areas

s t r e a m d i s s e c t i o n than
tend to have the most

they o v e r l i e b e dr o c k valleys,
for b u r i a l of ice.

NO R T H E R N D I ST AL REGION S
In distal
has

regions,

the O u t e r Port H u r o n o u t w a s h plain

flat to g e nt ly rolling t o p o g r a p h y p u n c t u a t e d by

n um e r o u s deep kettles,
valleys.

a few k e t t l e

U n a d j u s t e d g r ad ie nts

o u t w a s h surface

chains,

and m a n y dry

for the s o ut he ast

are a p p r o x i m a t e l y

3.1 m/km.

sloping

The Manistee

127

River
the

is at the distal

edge of the p l a i n and marks

so ut hw e s t w a r d route of former m e l t w a t e r drainage.

Is ola te d small hills

in the area are

i n t er pr et ed to be

p a r t i a l l y b u r i e d ou tl ie rs of the o ld er G r a y l i n g u pl and s
centered

farthe r east

(Fig.

32).

Lakes of the N o r t h

margin

A series of small,

s c a tt er ed al luvial

(Fig.

(Secs 9,

10,

T.

29 N . ,R.

5 W.)

fans of o u t w a s h

32) wit h p r o x i m a l l y feeding d i s i n t e g r a t i o n ridges

att a i n a l t it ud es
Resort,

about

of 420 m near Lakes of the N or th

3 km distal

c o nt ac t slope.

to the O u t e r Port H u r o n

Sedi me nt s are coarse

textured,

ice-

with

bo ul d e r s c o n c e n t r a t e d on d i s i n t e g r a t i o n r i d g e s and along
ic e - c o n t a c t slopes.

A ltogether,

int er pr et ed as an ice marginal

these l a n d f o r m s

te rminus

are

fo r me d p r i o r

to

the main O u t er Port H ur o n position.

M U L T I P L E MARGI NS OF THE
S O U TH ER N O U T E R PORT H U R O N C O M P L E X
From M a n i s t e e

Lake southward,

the O u t e r Port H u r o n

Co m p l e x co ns i s t s of an as se mb la ge of m o s t l y small,
isolated heads of ou tw as h that c o l l e c t i v e l y m a r k five ice
ma rgi na l p o s i t i o n s
angles to ov era ll
di ag no st ic

(Fig.

32).

la nd f o rm trend

(Fig.

40)

sh o w the

im br ic at e- 1 ik e m o r p h o l o g y typic al

morphosequences

(Koteff and Pessl,

po ssi bl e e x c e p t i o n of p o s i t i o n
er osi on by sub se qu e nt me l tw at er
obs er v e d

Pr of il es d r a w n at right

1981).

1, all

of

W i t h the

show s i g n i f i c a n t

streams.

in the n o r t h e r n half of se ct i o n s

Th i s

is best

35 and 36,

T.

-

POSITION 4

NW

375 m

SE

POSITION 3

128

POSITION 1
POSITION 2

345 m
315 m

0

5

Figure 40. Profile across the Outer Port Huron Complex.

10 ml.

129
26 N.,
cut

R.

8 W . , where

into the base

a southwest-trending dry channel

of p o s i t i o n

five m a r g i n s are s h o w n
positions
s er i es

are

3.

in Ta bl e

C h a r a c t e r i s t i c s of all
7.

Toge th er,

i n t e r p r e t e d as t e r r a i n

of s uc ce s s i v e

marginally

is

these

five

formed a lo ng a

st a g n a n t

gl a c i al

terminii.

SUMMARY
The O u t e r

Port H u r o n crest m a rk s

an e s p e c i a l l y

i m p o r t a n t he a d of o u t w a s h that

is g r a d e d to the O u t e r

Port H u r o n o u t w a s h p l a i n

32).

moraine

fl a n k e d by di s t a l

(L e v e r e t t and Taylor,
Bell,

1982).

ice-contact
erosion,
ar e a s

(Fig.

The
slope,

Martin,

proximal

1955;

F a r r a n d and

u n m o d i f i e d by s u b s e q u e n t

meltwater

however.

Many proximal

fo rm e d by d i f f e r e n t i a l

d e p o s i t i o n of s u p e r g l a c i a l

sand and gra ve l

ma s s

Ov erall,

of u n e v e n thickness.

alo ng

in di ca te that

f r o m an ice

m o r p h o l o g y and

ice m a r g i n a l

the south,

a series of five

glacial

by othe rs

is a true

display hummocky topography

transitory toward

is not a

acclivity

in o n l y a few places,

sediments

it

o u t w a s h as m a pp ed

1915;

steep,

Thus,

p o s i t i o n s wer e

w i t h t e r r a i n here

successive marginally

more

formin g

stagnant

positions.

Conclusions
R e g i o na ll y,
are d i r e c t l y
Lar ge

s a l ie n t and r e e n t r a n t

r e l a t e d to s u b s u r f a c e

landform patterns

b e d r o c k t o p o gr ap hy .

s a l i e n t s are a s s o c i a t e d w i t h e x t e n s i v e b e d r o c k

TABLE 7. CHARACTERISTICS OF MULTIPLE ICE-MARQIHAL P0SITI0N6.
-Position
1

Morphology

Loaatlon
S o u th ern e x t e nsion
of m a i n O u t e r Port
Huron position

42-48 m relief,
closed depressions,
disintegration
ridges, perforation
features, h a ngin g
valleys, kettles

S e d i me nts
gla aio f l u v i a l sand
and g r a v e l ,
glaciolaoustrine
silt and clay,
ra n d o m b o u l d e r
distributions

2

Seo. 10, T.
R . .7 W.

26 N. ,

390 m in altitude,
landforms same as
position 1

gl a a i o f l u v i a l sand
a nd gravel, orestal
b o u lde rs

3

Seo. 36,
R. 6 W.

28 N . ,

30 m relief, 364 m
in altitude,
landforms same as
p osition 1

gl a c i o f l u v i a l sand
and gravel,
glaoiolacustrine
s l l t a n d clay,
orestal b o u l d e r s

T.

4

S e o e . 6 and 6,
T. 26 H. , R. 7 W.

69 m relief, 417 m
in altitude, h ighly
disseoted, landforms
same as position i

same as 3 b u t no
orestal bo ulders
observed

6

SE 1/4,
T. 26

36 m relief, 361 m
in altitude,
landforms same as
position 1

sam e as 4

pea.
, R.

33,
7 H.

131
lowlands,
valleys.

small er sa lients w i t h less ex te nsi ve
These,

of te r r a c e

in turn,

re mn a nt s

be dr oc k

are d i r e c t l y r e la te d to the size

(Camp Ten,

Alba,

and 612

surfaces)

a s s o c i a t e d w i t h ea c h salient.
The p r e s e n c e
slopes,

of

1) steep,

2) h a n g i n g valleys,

imbricate,

asymmetrical

proximal

3) p e rc he d

4)
and 5)

indicate that

Inner and O u t e r Port H u r o n Co m p l ex es

formed along m a r g i n a l l y

st agnant

ice c h a r a c t e r i z e d by

ab un da n t m e l t w a t e r and s u p e r g l a c i a l
de gl aciation,

fans,

t o p o g r a p h i c profiles,

w i d e s p r e a d d i s i n t e g r a t i o n l a nd fo rms
t o p o g r a p h y of the

ic e- contact

drift d u r i n g

in a f a shi on d e s c r i b e d by Pri ce

and B le we tt and R ie ck

(1973),

(1987).

Cr e s t s of bo t h the Inner and O u t e r Port H u r o n
t ren d more

than

final

50 km and m a r k

features

im portant h ea ds of o u twa sh

grad ed to the E l m i r a P l a i n and O u t e r Port H u r o n o u tw as h
plain,

respect ive ly .

The no ti o n that ea c h feature

mo ra in e wi th d i s t a l l y flanki ng o u tw as h
D es p i t e

such similarities,

b e t w e e n the two
H u r o n pr ox i m a l
slope,

features.
acclivity

is a

is unsup por ted .

m a j o r d i f f e r e n c e s exist

In most places,

the

Inner Port

is in t e r p r e te d as an ice -contact

w h e r e a s the O u t e r Port H u r o n bluff has been

modified

s i g n i f i c a n t l y by s u b s e q u e n t m e l t w a t e r erosion.

Pr ox i m a l

zones

in the O u t e r Port H u r o n

and more v a r i a bl e

than c o r r e s p o n d i n g

Inner Port H u r o n margin,

and on l y the

c o n t r o l l e d d i s i n t eg ra tio n.

feature are w id er

tracts

along the

form er e x h i b i t s

In addition,

the br oa d

o u t w a s h pla in s of the O u t e r Port H u r o n C o m p l e x co ntrast

132

sh a r p l y w i t h the n a r r o w va l l e y t r a i n a s s o c i a t e d w i t h the
Inner Port H u r o n position.
L e v er e tt and T a y l o r ’s M a n c e l o n a Pl ai n con ta in s
principal
wi t h

e q u i l i b r i u m ou t w a s h su rf a c es

8 r ec og ni z ed a n c i l l a r y terraces.

are extensive,
hundreds

Su rf a c e s

T h e i r great

of as so c i a t e d de po s i t s

formed over a r el at i v e l y long

a n c i l l a r y te rraces c ov er li mit ed areas and,
reg io na l

la n d f o r m patterns,

conditions,

In contrast,
based on

from glaci al

c h a r a c t e r i z e d by rapid

falli ng w a t er tables.

they

most p r o b a b l y mark a

r e l a t i v e l y brief t r a n s i t i o n p e r i o d
gl aci al

covering

size and the

indica te that

time period.

along

1 and 2

r eg io n a l l y s i g n i f i c a n t la n d f o r m s

of square kilometers.

thickness

(1 and 2),

two

to n o n ­

in ci si on and

Ch ap te r 4
P R O P O S E D D E G L A C I A T I O N AND
L A N D F O R M D E V E L O P M E N T IN THE STUDY AR E A

Final d e g l a c i a t i o n events

are di v i d e d

into

six

s ucc ess ive phases:

1.

F o r m a t i o n of the Out er Port H u r o n Complex;

2.

F o r m a t i o n of s urface

3.

F o r m a t i o n of the Inner Port H ur on Complex;

4.

F o r m a t i o n of the Post

5.

1;

Inner Port H u r o n zone;

F o r m a t i o n of d i s i n t e g r a t i o n t o p o g r a p h y west
Kalkaska;

of

6. P o s t g l a c i a l m o d i f i c a t i o n of the landscape.
As d i s c u s s e d

in Ch ap ter

2,

final d e g l a c i a t i o n was

c h a r a c t e r i z e d m a i n l y by thick g l a c i o fl uv ia l
u p o n an u n e v e n cla y
(Fig.

13).

The

surface

sub cr op pi ng

in cl in ed tow ar d the northwest
sed iment

that was d e p o s i t e d either du ri n g
an d/ or retreat,
glaciation

deposition

is p r o b a b l y till

1) Port H u r o n advan ce

or 2) an e a rl i e r Late W i s c o n s i n a n

(Port Bruce?).

Two mo des

of d e p o s i t i o n most lik el y ac co u n t

p a t t e r n of o v e r l y i n g g l a c i o f l u v ia l

sediments:

1) In fi lli ng a lo ng a quasi-stable,
glacial p o s i t i o n (Fig. 41a), or

marginally

2) D e p o s i t i o n along a s t e a d i l y r et rea ti ng
(Fig. 41b).
Evi den ce p r e s e n t e d be low
mod els ma y ac co un t

indicates

for d e g l a c i a t i o n
133

for the

stagnant

ice mar gi n

that as p e c t s

of both

in the s t u d y area.

134

Time 1
Time 3

ICE

Figure 41A

Tim* 1
Tim* 1

ICE

ICE

Figure 41B

Figure 41. M odels of deposition for
the M ancelona Plain

135

The p r e c i s e m a x i m u m p o s i t i o n of Port H u r o n
c a nn ot

ice

be d e t e r m i n e d on the b a s i s of m o r p h o l o g y and the

li m i t e d

sedimentological

reason,

i n t e r p r e t a t i o n s of d e g l a c i a t i o n b e g i n w i t h

f o r m a t i o n of the ol de s t

d a t a av ailable.

recognized

in the O u t e r Port H u r o n Complex.
however,

have

similarities
Complexes

advanced

in re gional

and

and T a y l o r

east,

tr en d s

and Bell

(1982).

(1915),

Events

e v i de nc e

successive

5 -1,

presented

(1955),

42,

i n d i c a t i v e of

su bgl ac i a l

these

la n d f o r m s

so ur c e s

by s u p e r g l a c i a l

se ct i o n s

meltwater

from

of c u t w a s h .

m a n y or i e n t e d
also

form ed w i t h i n

w h i c h u s u a l l y are

drainage,

Th e i r a b s e n c e m a y be e x p l a i n e d

ma r k a se ri e s of

in s o u t h e r n

Here,

ice terminus,
Eskers,

di sc us se d

1.

C o n t r o l l e d d i s i n t e g r a t i o n ridges,

ice.

an d F a rr an d

in p r e c e e d i n g chapters.

y o u n g e r m a r g i n s has e r od e d o l d e r h e a d s

of s t ag na nt

by

s t r a t i g r a p h i c , and

shown in Fig.

the O u t e r Po rt H u r o n Complex.

areas

s u p p o r t e d by

of final d e g l a c ia ti on ,

ice m a r g i n a l p o s i t i o n s

p e r p e n d i c u l a r to the

ice may,

u p la nd s as m a p p e d

Martin

Ph ase
Positions

a vi e w

landforms

of the Port H u r o n

are b a s e d on mor pho lo gi c,

chronologic

ice ma r g i n a l
Port H u r o n

the o l d e r G r a y l i n g

Le v e r e t t

below,

f ar th er

For this

are not

identified.

e i t h e r by 1) bur ia l
drift,

of

or 2) m e l t w a t e r

that were p r i m a r i l y s u p e r gl ac ial .

In contrast,
margin remained

to the n o r t h the p o s i t i o n of the
r e l a t i v e l y stable.

That

is,

after

ice

of

136

DIRECTION AND RELATIVE
AMOUNT OF ICE-MARGINAL
RETREAT
DIRECTION OF
MELTWATER DISCHARGE

Lakes of the
North margin

Figure 42. P h ase 1. Formation of the
Outer Port Huron Com plex

137
forming the Lakes of the N or th o u t w a s h aprons,
glacial

ma rg in re tr ea t e d to the m a i n Ou ter Port H u r o n

p o s i t i o n early
of

in phase

ice-m ar gi na l

As a result
pro mi ne nt

1, and did not p r o d u c e

land fo rm s

s i mil ar to those

the t o p o g r a p h y here

and may have

features,

n o rt he rn areas e xh ibi t

r e l a t iv e ly

sou t h er n region,
smaller,
ma r k i n g

This

rotat ed cloc kwi se
42).

centuries.

of the N o r t h

a c c l i v i t y formed alo ng
sta gna nt

co nt ain s

ice margin.

of

of o u t w a s h

st ag nan t glaci al

that the

to the no r t h we st

a

The

an a s s e m b l a g e

less pr o m i n e n t h ea ds

indicates

and

an ex te ns iv e o u t w a s h

five s uc ce ssi ve m a r g i n a l l y

positions.

(Fig.

stable,

however,

separate,

f a rt he r south.

formed w i t h i n several

p la in w i t h a steep pr ox im al

a series

is both d i s t i n c t

W i t h the e x c e p t i o n of the Lakes

single,

the

ice m a rg in p r o b a b l y
duri ng

deglaciation

T e rr ac e pa tt e r ns on the M a n c e l o n a P l a i n

indicate that this style of ma r g i n a l

retrea t was

c o n f i n e d to the O u t e r Port H u r o n Complex,
characterized deglaclation throughout

not

but

southern

r e gi on s of

the study area.
H u m m o c k y pr ox i m a l

tracts

in the O u t e r Port H u r o n

Co mp l e x d i s p l a y c o n t r o l l e d and u n c o n t r o l l e d
d i s i n t e g r a t i o n t o p o g ra p h y c o m p o s ed
s tr a t i f i e d drift.
at tr i b u t e d

Ch ur c h

(1972)

fo rm at i on of si mil ar

g l ac io fl uv ia l

i c e- co nt ac t

and Price
lan df or ms

ou tw as h plains or ig i n a t i n g on the
dis ta nc e up-ice

of

to

ice s u rfa ce a short

from the glacial margin.

sediments

(1973)

Likewise,

of the O u t e r Port H u r o n ou twa sh

133

pl ai n were p r o b a b l y depo si te d ov e r a r e l a t i v e l y thin
layer of stagna nt

ice,

which,

up o n melting,

pr o d u c e d the

p r o x i m a l h u m m o c k y t op og ra ph y o b s e r v e d today.
The

1) al i g nm e nt

M a n c e l o n a Pl ai n with

of er o de d terrace
tr uncated pr ox im al

Port H u r o n r een tr ant s
c re st al

(Figs.

bo ul d e r s along

H u r o n Complex,

32,

33),

2) absen ce

true

ice-con ta ct

p o s i t i o n of the
modified

of

of a bo ul de r lag along the

base of the O u t e r Port Huron p r o x i m al
in most p l a c e s

slopes of Outer

large se gm e n t s of the O u t e r Port

and 3) pr esence

that

scarps on the

slope

indicate

the Ou te r Port H u r o n bluff

slope.

Although

ice margin,

this

is not a

it marks the general
a c c l i v i t y has been

s i g n i f i c a n t l y by m e l t w a t e r erosion.

N u m er o us h an gin g valleys are also a s s o c i a t e d with the
crest of the O u t e r Port H u r o n
m e l t w a t e r er o s i o n

feature,

increased just p ri or to a b a n d o n m e n t of

the Ou te r Port H u r o n Complex.
a s s o c i a t e d with stagn at in g
v i g o r o us

over time,

d ec re a s i n g

im plying that

se diment

v e r y last m e l t w a t e r

this

B e ca us e m e l t w a t e r

ice u s u a l l y beco me

streams

less

i n c i s i on likely re fl ect s a

supply.

Th es e v a lle ys must ma r k the

streams,

otherwise

they w o u l d have

be en al ter ed by later events.
M e l t wa te r
d iv e r t e d
(Fig 42),
M a ni st ee

from the Outer Port H u r o n C o m p l e x was

so ut hwe st by the o l d e r Lake Border M or ai ne
fo llowing
River.

a course

Burgis

s i mil ar

(1977)

to the m o d e r n

c or re la te s the a ss oc ia te d

o u t w a s h surfaces w i t h the G l e n w o o d

II Stage of Lake

139
Chicago

in the Lake M i c h i g a n basin.

A c o m p l e x p r o g r e s s i o n of pr og l a c i a l
b e t w e e n the

ice and the O u t e r Port H u r o n

s ou th as the g la ci al
t hei r

size,

lakes

ter minus was

formed

slope

in the

rotating northwestward,

de pth and al titude being co nt ro ll ed by

p o s i t i o n i n g of the
re tr ea t op en ed

ice margin.

lower outlets,

Furth er ic e- ma r g i n a l
d r a i n e d the lakes,

and

ini ti at ed m e l t w a t e r dr ai na ge on the C r of t o n o u t w a s h
s ur fac e

(Fig.

43).

Phase
Eve ntu al

d e g l a c i a t i o n of the m a i n p o s i t i o n farthe r

no rt h

initi ate d

Huron

slope,

terraces,

2

fosse dr ainage proxim al

forming

Fig.

44).

surface

to the O u t e r Port

1 (Camp Ten,

Alba,

and

612

The c o r r e s p o n d i n g p o s i t i o n of the

ice m a r g i n a s s o c i a t e d wi t h this

surface

(Fig.

44)

is

i n t e r p r e t e d on the basis of the

fo llowing evidence:

1) becaus e the three te rr ace s are re mnants of
surfac e 1, the latter must, have been more extensive.
Such di me ns i o n s require a prominent, r e g i o n a l l y
si g n i fi ca n t h e a d of o u t w a s h some wh ere p r o x i m a l to
the O u t e r Port H u r o n Complex.
2) It is u n l i k e l y that this ice ma r g i n was locate d
at the Inner Po rt H u r o n p o s i t i o n becaus e su rfa ce 1
w o u l d have had to cover the entire M a n c e l o n a Plain.
S u b se q ue nt f o r m a t i o n of the lower El m i r a s u rf ac e
w o u l d r e qu ire the e r os io n of a sediment vo lu m e
a v e r a g i n g 15 m thick, 75 km long and 6 k m wide, an
amou nt that seems ex ce ss iv e giv en es ti ma te s of
p a l e o d i s c h a r g e (this study) and age c o n s t r a i n t s for
Port H u r o n e v e n t s from o th er studies elsewhere.
3) a bo uld er lag on the Elm ir a surface, just
p ro x i m a l to the Al b a and Camp T e n scarps, p r o b a b l y
ma rks the for mer ice ma rg i n a l position.
Th i s
e x p l a n a t i o n a s s u m e s that E l m i r a m e l t w a t e r streams
have eroded the ice -marginal p o rt io ns of the two

140

DIRECTION AND RELATIVE
AMOUNT OF ICE-MARGINAL
RETREAT

DIRECTION OF
MELTWATER DISCHARGE

Lakes of the
North margin

Crofton surface

Figure 43. Formation of th e Crofton surface

141

DIRECTION OF
MELTWATER DISCHARGE

Lakes of the
North margin

Crofton
surface

Figure 44. P h a s e 2. Form ation of Surface 1.

142
terraces.
B o u l d e r s c o n c e n t r a t e d at the g l ac ia l
m a r g i n we r e too large for s t r e a m tr a n s po rt and
r e m a i n e d as r e s i d u a l s that d e li m i t the f o r m e r ice
position.
Th is

ev i d e n c e

w i t h Phase

suggests

that the

2 be p l a c e d

somewhere

I nne r Port H u r o n posit i ons .
her e

s up po rt s

the

If correct,

terminus

Pha se

resulted

in 1)

su rf a c e

1,

scarps,

and 3)

45).

2)

re tre at

the

thickness,

d e p o s i t i o n on

of e r o s i o n on the

valleys,

Co mp le x

possibly lasting

su gg es t

se ver al

and

erosion,

6)

fans,

evidence

i nd ic at e

1)

that

5)

F a r r a n d and E s c h m a n

Manis tee ,

in Fig ur e

ice-contact

for m i n i m a l

fo l l o w e d
41a.

The

stratified

3) d r y ha ngi ng

subsequent meltwater

the Inn er Por t H u r o n p r o x i m a l

(1974)

ice-contact
tr ace

(1977)

slope.

the E l m i r a surfac e

the M a n c e l o n a Plain)

and B u rg is

centuries.

fe ed in g d i s i n t e g r a t i o n

d e c l i v i t y is in mos t p l ac es an

(which they call

sho wn

boulder concentrations,

4) p e r c h e d

(Fig.

an d v o lu me of s e d i m e n t s

in f i l l i n g m od el

2) cr es t a l

terrace

an e q u i l i b r i u m p e r i o d of

l o c a t i o n and d i s t r i b u t i o n of

ridges

In ne r Port H u r o n po s i t i o n

d e p o s i t i o n of E l m i r a s e d i m e n t s m ay have

successive

drift,

3_

Inn er Port H u r o n

s i g n i f i c a n t durat ion ,

the

m a rg in

41b).

f o r m a t i o n of the E l m i r a P l a i n

it form ed d u ri ng

If so,

to the

an u n k n o w n amo un t

The extent,

a glacial

(Fig.

the end of g l a c i o f l u v i a l

a s s o c i a t e d w i t h the
th at

b e t w e e n the O u t e r and

idea that d e p o s i t i o n oc c u r r e d a l on g a

s t e a d i l y r e t r e a t i n g gl ac ia l

Ice ma r g i n a l

ice m a r g i n a s s o c i a t e d

correlates

southwest

to

it w i t h the

143

DIRECTION OF
MELTWATER DISCHARGE

C am p Ten
surface
Alba surface

'

Lakes of the'
the North margin

612
surface

v

Crofton
surface

Figure 45. P h a se 3. Formation of Surface 2.

144

Glenwood

II stage of Lake Chicago.

the Inner Port H u r o n Complex,
we r e opened,
46).

W i t h d e g l a c i a t i o n of

lower m e l t w a t e r outle ts

and the Elm ir a Pla in was a b a n d o n e d

Su rf a c e s

3,

4,

and 5 m a r k the tr an s i t i o n

(Fig.

to these

lower outlets.
The
2)

1) p a t t e r n of su rfaces

3,

4 and 5 (Fig.

32)

r e l a t i o n s h i p of these su rfaces w i t h the small

valle ys

described

marginal

re tr ea t

progressed

in C h a p t e r

4 indicate that

and

incised

ice-

from the Inner Port H u r o n C o m p l e x

from south to north,

thus

c on ti nu in g the

p r e v i o u s l y e s t a b l i s h e d n o r t h w e s t w a r d pi vo t i n g m o t i o n
(Fig.

46).

Ne a r M a n c e l o n a

(secs.

W . ), h e a d w a r d p o r t i o n s of some

5 and 6, T.

29 N.,

R.

6

incised dry ch an n e l s

car ve d by s u p e r g l a c i a l m e l t w a t e r are nearl y 70 m above
the base of the

ice-con ta ct

s o u t h e a s t w a r d onto
its surface.

slope.

These c h a n ne ls extend

the E l m i r a P la in and are

into

T h e i r d o w n s t r e a m ends e v e n t u a l l y m e r g e with

the c o m p l i c a t e d terrace a s s e m b l a g e m a r k i n g
and 5.

i n ci se d

If th es e

latter su rf ac es are

su rf a c e s

3, 4,

followed

s o u t h w e s t w a r d , t he ir d o w n s t r e a m po rt i o n s

lie p r o x i m a l

the Inner Po r t H u r o n ic e - c o n t ac t slope.

Thus,

streams d r a i n i n g
position west
farther south.
la ndforms

the

m e l tw at er

ice m a r g i n at the Inner Port Huron

of M a n c e l o n a

lie pr ox im al

to this ma rg i n

In c o m b i n a t i o n the a r ra n g e m e n t of

suggests

Hu r o n p o s i t i o n we s t

to

that

these

ice r e ma in ed at the In ner Port

of Mancelona,

wh il e a si mil ar

p o s i t i o n a l r e a d y had been a b a n d o n e d

farther

so uth

(Fig.

145

DIRECTION AND RELATIVE
AMOUNT OF ICE-MARGINAL
RETREAT
DIRECTION OF
MELTWATER DISCHARGE
C am p Ten
surface
Alba surface

Lakes of the,
North margin

SURFACE 4
612
surface
SURFACE 3

SURFACE 2

Crofton surface

Figure 46. Formation of su rfaces 3 a n d 4.

146

46).

Such a p a t t e r n

is c o n s i s t e n t w i t h

fro m the O u t e r Port H u r o n feature,
terminii
Burgis

where

likewise pivoted northwestward.

(1977)

northeastern
north

i n te r p r e t a t i o n s
southern
Int er es ti ng ly ,

found that Port H u r o n d e g l a c i a t i o n
southern Michigan progressed

in a s i m i l a r

fashion,

except

in

from s o u t h to

there the

ice m a r g i n

l o ca t e d at the

In ne r Port

r o t a t e d n o r t h e a s tw a rd .
The H o f f m a n Lak'- Channel,
H u r o n apex,
this

is cut d e e p l y

lat te r s u r f a ce

is not

into

the E l m i r a Plain,

incised

i m m e d i a t e l y to the

south.

If an

ice m a r g i n was p o s i t i o n e d along the

contact

slope

at t h e s e

two l o c a t i o n s

Th i s

r e m a i n e d at the a p e x a ft er a re as
already deglaciated

(Fig.

H o f f m a n Lake C h a n n e l
east, must have b e e n
Channel

retreat

ice

f a rt he r so ut h we r e
Because meltwater

ice free.

Thus,

in the

the a r e a to the

the H o f f m a n

Lake

fo r m a t i o n of the E l m i r a s u rf a c e and
a p e x ’s e a s t e r n side,

from the w e s t e r n edge

O n these bases,

in ci se d the

su gg e s t s that

dr a i n e d east wa rd,

for me d a f t e r

d e g l a c i a t i o n of the

47).

ice-

contemporaneously,

t h e n the a s s o c i a t e d m e l t w a t e r w o u l d have
E l m i r a s u rf ac e at b o t h places.

yet

(Fig.

the H o f f m a n Lake

i n t e r p r e t e d as h a v i n g

Burgis

be fo r e

47).
f ea tu re

formed v e r y late

H u r o n d e g l a c i a t i o n sequence.

but

in the

(1977),

is
I n n e r Port
studying

Po r t H u r o n M o r a i n e

in n o r t h e a s t e r n Michigan,

c o n c l u d e d that the

Inner Port H u r o n apex wa s the

r e g i o n to be d e g l a c i a t e d d u r i n g

also
last

Port H u r o n retreat.

the

147

Hoffman Lake
Channel

DIRECTION AND RELATIVE
AMOUNT OF ICE-MARGINAL
RETREAT
DIRECTION OF
MELTWATER DISCHARGE
Cam p Ten
surface (1)

Alba surface (1)

Lakes of the,
North margin

SURFACE 4
SURFACE 3

612
surface

SURFACE 2
•Crofton
suriace

Figure 47. Formation of surface A.

148

There
Channel

is the p o s s i b i l i t y that the H o f f m a n Lake

for med

from d r a i na ge of G r e a t l a k e a n / V a l d e r a n

ice

that had r e a d v a n c e d to p o s i t i o n s m a r k e d by the apex.
M el hor n

(1954)

and Burgis

(1977),

however,

both map the

G r e a t l a k e a n / V a l d e r a n b ou nd ar y no rth of the apex,
su gge st ing

that

this advan ce did not reach the proximal

border of the Inner Port H u r o n C o mp le x here.

Phase
As the m a r g i n w i t h d r e w
position,
Port H u r o n
s ed iments

proglacial

lakes

i c e - co nt act

from the

formed pr ox ima l

slope.

of

12,960

the ice m a r g i n wa s p r o x im al

ou t w a s h s u r fa ce s

C,

(Fig.

and D.

retreat,

(A-H,
47)

Pit),

from

lakes y i e l d e d a
(TX-6151;

IV
C

Ant ri m

and i n d ic at es

that

to the Inner Port H u r o n

W - Z ) wer e

formed,

b e g i n n i n g with
surfaces

T o g e t h e r w i t h te rr ac es E-H2 and W-Z,

b ra ide d c ha nn e l

from a single,

J o r d a n - W a r n e r valleys;

m e l t w a t e r d o m in at ed

systems

Fig.

(C ed ar - Gr ee n and

48).

is c l o s e l y r e l a t e d to surfaces

(Elmira Plain).

they

to two sep ara te p r e c i p i t a t i o n / g r o u n d w a t e r

single channe l

S ur fac e A

a s u c c e s s i o n of lo we r

and fo ll ow ed by inc isi on of

record the t r a n s i t i o n

co nt r o l l e d

B.P.

Inner

this time.

Wi th c o n t i n u e d

B,

to the

Or gan ic m at er ia l

± 350 yrs.

Cou n t y Road C o m m i s s i o n Gravel

surface A

Inner Port Hu ro n

a s s o c i a t e d wi t h one of these

age es ti ma te

Compl ex at

4.

All

are extensive,

s ig ni fic ant d e p o s i t i o n a l

features

1 and 2

re gi on a l l y

c o n t ai ni ng

thick

149

Hoffman Lake
channel

Jordan/Warner
riversystem
Cam p Ten
surface (1)

Cedar/Green
riversystem

valleys

X!

Lakes of the
North margin

612
surface
Crofton
surface

Figure 48. Formation of the Jordan-Warner and
Cedar-Green river system s.

150

ou tw a s h d e p o s i t s
margin.

formed along a r e l a t i v e l y stable

In s t ri ki n g contrast,

s m al le r features.
deglaciation

l o w e r terraces ar e much

T h e y re p r e s e n t a c o m p a r a t i v e l y brief

interval c h a r a c t e r i z e d by falling

levels cau sed by openin g of lo we r outlets,
co n c o m i t an t dr op

in w at er tables.

v e r y c o m p l i c a t e d b e ca us e of the
remnants,

2) p o o r c h r o n o l o g i c

g l a c i o f l u vi al
lake levels
role

ice

surfaces,

base

wi t h a

R e la ti ons hip s

here are

1) pa u c i t y of t e rr ac e

c o n t r o l on fluvial

and

3) li mi t e d knowledge of related

in the Lake M i c h i g a n bas in and 4) u n c e r t a i n

(if any)

of G r e a t l a k e a n / V a l d e r a n ice in st re a m

history.

Phase _5
Sometime a ft er
Huron position

form at ion of the Post

(perhaps during

G r e a t l a k e a n / V a l d e r a n advance)
readva nc ed

to the

C h a p t e r 4,

d o w n s t r e a m po rt i o n s

along wi th pa rts
o v e r r i d d e n by
in secs.
T.

27 N.,

includes

the subsequent
th e

ice ma rg i n in pl ac e s

Inner Port H u r o n crest.
of surfaces

As n o t e d
3,

4,

in

and 5,

of the Post I nn er Port H ur on zone,

were

ice and then b u r i e d by sta gn at io n deposit s

35 and
R.

Inner Port

36,

8 W.

T.

(Fig.

28 N . , R.
49).

8 W. , and secs.

E v id en ce

1 and 2,

for burial

1) an abrupt d o w n s t r e a m t e r m i n a t i o n of wide,

g e nt ly sloping,

low relief o u t w a s h surfaces by

un c o n t r o l l e d d i s i n t e g r a t i o n topography,
w i t h i n these d i s i n t e g r a t i o n tracts
to c orr ela te w i t h su rfaces

3,

4,

and 2)

al titudes

that are mu c h

too high

or 5. Burial must post-

151

Hoffman Lake
channel

LIMIT OF POST INNER
PORTHURON ZONE

a
Cam p Ten
surface (1)

J
Alba su rfa c e (l)
Through
valleys

v
Lakes of the
North margin

612
surface

Crofton
surface

Figure 49. R eadvance after formation
of the P ost Inner Port Huron zo n e.

152

date Phase

3 and 4 and r e f l e c ts

f l u c u at io n s d u r i n g

(Fig.

Phase
T o p o g r a p h y in the
alteration,

int eg r at ed d r a i n ag e

due

westward

ru no f f

networks.

e vi de nc e
l i ke ly
water

wi t h n u m e r o u s

fa vo rin g the
An

important

f o r m at io n of
exception

tributary valleys

15 m
trends

to the

The o r i e n t a t i o n of the l o wl an d a n d lack of

a superglacial
for spring

formed

its u p s t r e a m end

meltwater

sappin g

source.

is observed.

i m m e d i a t e l y fo l l o w i n g

tables were m u c h higher,

e ff lu en t

to the h i g h l y p e r m e a b l e

w h e r e a flat bottomed,

an a s s o c i a t e d ha n g i n g v a l l e y at
pr e c l u d e s

49).

from the O u t e r Port H u r o n C o mp l e x d o w n

E l m i r a Plain.

or 2)

6.

in pa r t

exi st s at the A l b a salient,
dry channel

i c e - m ar gi na l

s t u d y a r e a has e x p e r i e n c e d little

sa nd y drift w h i c h limits

deep,

1)

final Port H u r o n de gl ac iat ion ,

G r e a t l a k e a n / V a l d e r a n a d van ce

Ho l o c e n e

eit he r

to this

tables dropped,

No

Thi s v a l l e y

deg la ci at io n,

p r o v i d i n g lar ge

s t r e a m system.

As

whe n

am oun ts

ice w i th dr ew,

p e r h a p s pr ec ip i t o u s l y ,

brief per io d of in c i s i o n by th ese

spring or

wa te r

a c c o m p a n i e d by a

streams.

Elsewhere,

this pr oce ss p r o d u c e d onl y li m i t e d d i s s e c t i o n al ong
O u t e r Port H u r o n m a r g i n and su rf ac e
West of Alba,
in la cu st ri ne
overlook.

(?)

Here,

the west and more

a spectacular
cla y

1 te rr ac e

example

of

the

scarps.

of s p r i n g - s a p p i n g

is o b s e r v e d at the L a n d s l i d e Creek

an a m p i t h e a t e r - l i k e
tha n 50 m deep,

hollow,

concave

forms the h e a d w a t e r

to

153
r e g i on of L a n d s l i d e

Creek.

conspicuous

of the w i d e s p r e a d H o l o c e n e

example

sapping occurring

This

throughout

feature

is the most

tr ac t s pro xi ma l

spring-

to the

Inner

Port H u r o n Complex.
S t r e a m piracy,

a u g m e n t e d by sprin g- sap pi ng,

is

an im po rta nt p r o c e s s

in the C e d a r - G r e e n and J o r d a n - W a r n e r

Creek

st re ams

systems,

where

In ner Port H u r o n
seq u e n ce

in secs.

headward portions
to

hea dw ar d

into the

s lo pe have p r o d u c e d a c o m p l i c a t e d

of H o l o c e n e

displayed

cu t t i ng

drainage

27 and 28,

diversions.

This

T.

6 W . , where

30 N . , R.

of the C e d a r R i ve r

the Inner Port H u r o n bluff)

have

is best

(oriented p ar al le l
been c a p t u r e d by

G r e e n River and C a s c a d e C r e e k

(ori en te d p e r p e n d i c u l a r to

the

These

Inner Port H u r o n slope).

gr a d i e n t

stream networks

Inner Port H u r o n

streams

ice-contact

Regional

the o ut er l i m i t s

in areas p r o x i m a l
slope.

that the Port H u r o n Mo r a i n e

of a s i g n i f i c a n t gl aci al

his e vi d e n c e b a s e d p r i m a r i l y on the
mo r a i n e

to b e a c h e s

W hi t tl ese y.

This

a l t i t u d e gl aci al

to

correlation

In 1905 T a y l o r p r o p o s e d
marks

hi gh e r

m a y be e x p e c t e d to e x p a n d at the

e x p e n s e of lower g r a d i e n t
the

latter,

of g l a c i a l

advance,

r e l a t i o n s h i p of the

lakes A r k o n a and

i n t e r p r e t a t i o n p o s t u l a t e d that a lowlake,

Lake Arkona,

o c c u p i e d the

so ut h e r n

pa r t of the Lake H u r o n b a s i n p r i o r to fo rm at io n of the
Port H u r o n Moraine.

Advance

southeastern Michigan ponded

of Port H u r o n
the wa te r s

ice

into

of Lake A r k o n a

154
and

formed a new,

Tay l or
be ac h

(1905)

higher altitude

lake,

Lake Whittlesey.

d o c u m e n t e d t r u n c a t i o n of Lake A r k o n a

features by the mo r a i ne and

showed that Lake

W h i t t l e s e y was p e n e c o n t e m p o r a n e o u s with the Port H ur on
fe a t u r e .
M od e r n
(Fullerton,

studies c o n f i r m T a y l o r ’s in ter pre tat ion s
1980).

Age d e t e r m i n a t i o n s a s s o c i a t e d with

the rise and s t a b i l i z a t i o n of Lake W h i t t l e s e y
Ontario

and Ohio

yield

G o l d t h w a i t , 1958),
and 12,800 + 250
(1957).

12,900

(Y-240;

+ 200

12,920 + 400

(1-3175;

Barendsen,

13,000 y r s . B.P.

in the G re at

Ta y l or

(1913)

Lakes

(W-430;

Calkin,

Deevey,

Based on some of these dates,

a s s i g n e d an age of
advan ce

ages of

in

1970),

and Gralenski

Hough

(1958)

to the Port H u r o n

region.

c o r r e l a t e d the Port H u r o n M o rai ne

in s o u t h e a s t e r n M i c h i g a n wi t h the W yo mi ng M o r a i n e
s o u t h w e s t e r n Ontario.

W o o d a s s o c i a t e d wi t h St.

in

Jo s ep h

IU

till
of

from the W y o m i n g Mo r a i n e y i e l d e d a

13,000

+ 100 yrs.

B.P.

Stupavsky,

1976;

co r r e l a t e s

this till w i t h

(GSC-2213;

L o w d o n and Blake,
"Jeddo

C age es timate

Gr av e n or and

1976).

till"

Eschman

from the Port

H u r o n Moraine:
It seems c e r t a i n that the J ed do till is the M i c h i g a n
e qu iv al en t of the St. J o s e p h till of On t a r i o -- each
is the surfa ce till in the t e r m i n a l m o r a in ic syst em of
Port H u r o n age, an d that s y s t e m has only a r e l a t i v e l y
narrow gap in it in the Port H u r o n - Sa rn i a re g i o n
(Eschman, 1978, p. 37).
Thus,

the age of the Port H u r o n M o r a i n e

M i c h i g a n is b a s e d on

|U
C dates

in s o u t h e a s t e r n

a s s o c i a t e d wi t h

155
morphologic

and s t r a t i g r a p h i c un it s

from o u t s i d e

of the

state that a p p a r e n t l y co r r e l a t e w i t h the f e a t u r e ’s type
area.

C o r r e l a t i o n w i t h i n M i c h i g a n -- T a y l o r
p r e se nt ed the

pl at e

II)

first map l i nki ng the Port H u r o n Mo ra i n e to

t op og rap hic

fea tu re s

Peninsula.

L e v e r e t t ’s 1911

formations

(1899,

shows

in the

n o r t h e r n part of the Sou th er n
map of the surfi cia l

the Port H u r o n Morain e

tre nd in g

from its

type area near Port Hu ron n o r t h w e s t w a r d to Muskegon.
Description,

cor relatio n,

and

i n te rp r e t a t i o n of the

feature w i th in M i c h i g a n was p u b l i s h e d by Le v e r e t t
Tay lo r

and

in 1915.

Blewett

( 1989 ) rev ie we d

c o r r e l a t i o n and

i de nt i f i e d

the basis for this
four prin ci pa l

criteria

used

by Leveret t and Taylor:
1. PATTER N -- the mo ra i n e (as map pe d by Lev erett)
nearl y c o n t i n u o u s across the state.
2. FORM —
the mo rai ne is a con sp ic uo us
feature, hig h and rugged in some areas,
subdued in ot he r s
3. A S S O C I A T I O N

is

topographic
low and

--

a. the m o r a i n e lies " i n s i d e ” of the o l d e r West
B ra nc h-L ake B o r d e r Complex;
b. the m o r a i n e is d i s c o r d a n t wi t h the W e s t B r a n c h Lake Bord er Complex;
c. the m o r a i n e burie s
so ut he as te rn Michigan;
d. the m o r a i n e
Whittlesey;

Lake Ark on a be ac h e s

in

is coeval w i t h beache s of Lake

e. near Lake M i c h i g a n the morain e is re l a t e d to
lakes dee me d c o r r e l a t i v e wi t h Port H u r o n even ts
in the H u r o n - E r i e basins.

156

4. L I T H O L O G Y -- the m o ra in e is d e l i n e a t e d us in g
t e x t ur ed s e d i m e n ts in the S a g i n a w lowland.
B ase d on n ew ly a v a il ab le top og ra ph ic

quadrangles,

soil maps,

and ae ri a l phot og rap hs,

r ec og ni z ed

five sub uni ts w i t h i n the morain e

sh ar pl y in m o r p h o l o g i c
cha ra ct eri st ics ,
corr elations,
qu es ti o n e d

topography

Blewe tt

(1989)
that differed

and se di me n t o l o g i c

and ob se r v ed that

Le verett and T a y l o r ’s

t h o u g h g e n e r a l l y accurate,

in some places.

These areas

n o r t h e a s t e r n s o u t h e r n Michigan,
continuous,

fine

can be
inclu de

w h e r e the

and 2) the Sa g i n a w lowland,
is p o o r l y developed.

1)

featu re

is not

w h e r e mo rainic

B l e w e t t ’s ana ly si s

c o n cl ud ed that age es ti ma te s and c o r r e l a t i o n of sediments
and te rr a i n

in n o r t h w e s t e r n s ou th er n Mi c h i g a n w o u l d

likely be e s t a b l i s h e d on the ba sis
dating.

Until

the presen t

study,

however,

for Late W i s c o n s i n a n or gan ic d e p o s i t s
part of the S o u t h e r n P e n i n s u l a we re
a l . (1969;

see next

Age d e t e r m i n a t i o n s
Michigan —
l acu str ine

in the no r t h e r n

limite d to Farran d et

section).

Inner Port Hu ro n Complex,

i m m e d i a t e l y pro xi ma l
about

6 W.).

12,960

site;

NW 1/4,

This m at er ia l

+ 350 yrs.

B.P.

to the

50 ra be low the crest

(Antrim Co un t y Roa d C o m m i s s i o n gravel pit,

R.

in northern

mat er ia l was re co ve re d from a

silt d e p o s i t e d

"Antri m County"

age estim ate s

for the Port H u r o n Co mp l e x

Organic

/V
C

of a p p r o p r i a t e

NW1/4,

sec.

he r e a f t e r
33,

T.

30 N.,

y i e l d e d a ,,fC age es t i m a t e of

(TX-6151).

Becaus e the

lake

157
a s s o c i a t e d w i t h these d e p o s i t s
b e t w e e n the

Inner Po r t H u r o n

f o rm ed

in a n a r r o w zone

ice-contact

slope

and an ice

m a r g i n l oc a t e d less t h a n a k i l o m e t e r to the northwest,
the silts must p o s t d a t e

the

In ne r Po rt H u r o n Complex.

The age and l o c a t i o n of t h e s e

s e d i m e n t s mean

In ner Port H u r o n C o m p l e x w i t h i n the
fo rm ed p ri or to

12,960

± 350 yrs.

for the

in ter pr et at i on ,

these d e p o s i t s

that

study ar e a

B.P.

m i n i m u m age e s t i m a t e

data

rath er

(E lmi ra

than clay,

The o l d e r Lake

An a l t e r n a t i v e

con tin ue
the

b e n e a t h the

feature,

surface)

at c o m p a r a b l e

Border Moraine

of the Port H u r o n C o m p l e x

altitudes.

is lo cat ed sou theast

in n o r t h w e s t e r n s o u t h e r n

and can be

tra ce d

southward

Illinois.

Fullerton

(1980)

a s s i g n e d an age of

yrs.

B.P.

to the complex,

an

into n o r t h e r n

( 13,870

640 yrs.

ISGS-1570;

c it ed

ISG S- 15 49

in H a n s e l

Glenwood

and Mic ke ls on ,

1987)

I stage of Lake Chicago,

ice m a r g i n a l
Il li no is

and

re tr e a t

(Fullerton,

1980).

14,000

yrs.

B.P.

Lin,

+

1987;

soon after

Border Moraine

in

estimates,

a m a x i m u m age

of

for the Port H u r o n Comple x
and,

A n t r i m C o un ty date,

the

A

14,100

a s s o c i a t e d wi th the

in n o r t h w e s t e r n s o u t h e r n Mic higan,
i n d i ca te s

C.L.

Ba sed on these

the Lake B o r d e r M o r a i n e p r o v i d e s
approximately

+ 170 and

w h i c h forme d

from the Lake

14,200 -

interpretation

s u p p o r t e d by r e ce nt ,4C d a t e s
B.P.;

the

show sand and

Michigan,

14,300

is not

from n u m e r o u s w el ls d r i l l e d along

Inner Port H u r o n cr es t
gravel,

likely

and e s t a b l i s h e s a

feature.

Inner Port H u r o n C o m p l e x and p r e d a t e
likely because

that the

that

c o m b i n e d wi th the
Inner a nd Outer

158

Po rt H u r o n C o m p l e x e s
and

14,000 yrs.

formed b e t w e e n a p p r o x i m a t e l y 13,000

B.P.

Farran d et a l . (1969)
b u r i e d by a sin gl e

12,570

± 500,

o t h e r ages
are

9,960

10,700

+ 400

W - 1 8 8 9 ; and

+ 350

+ 350

a short

(13,300

from the

a buri ed

red till n e a r Ch eboygan,

th a t a p p a r e n t l y m a r k s
b y three d a t e s

describe

same

Michigan,

interval

d e fi ne d

and

12,800

± 400,

12,500

+ 500,

W- 1847).

bed

(M-1753-1),

(M-1753-3).

ic e- f r e e

b r y o p h y t e bed

(Crane
10,700

The

L-1064;
Three

and Griffen,
± 350

1968)

(M1753-2),

first date was

and

r e j e c t e d by

F a r r a n d et a l . as being too young;

the o t h e r two were not

mentio ne d.

set of a s s u m p t i o n s

B a s e d on a c o m p l i c a t e d

p r e d i c a t e d by a c c e p t a n c e
bryophyte
int erval
th a t

of the o l d e r dates,

the

bed was a s s u m e d to r e p r e s e n t an ic e- f r e e
l a st in g

from about

13,000

to

12,500 yrs.

i m m e d i a t e l y p r e - d a t e d the Port H u r o n advance;

b e e n n am ed the C a r y - P o r t H u r o n

The

it has

till

overlying

the

r e p re se nt

u n i n t e r r u p t e d d e p o s i t i o n of till d u r i n g both

Di’y o p n y L e

be u was

interstade.

B.P.,

i n t e r p r e t e d to

the Port H u r o n an d G r e a t l a k e a n / V a l d e r a n substages.
ot h e r words,

a c c o r d i n g to F a r r a n d

In

et a l . 1) the

b r y o p h y t e s we r e b u r i e d by red till d u r i n g Po r t H u r o n
a d v a n c e to the m a x i m u m Port H u r o n position,
margin subsequently
not

2)

r e t r e a t e d d u r i n g Two C r e e k s

far e n o u g h n o r t h to u n c o v e r the b r y o p h y t e

3) G r e a t l a k e a n

ice th e n readvanced,

d e g l a c i a t i o n of the

the

time,

but

region,

and

followed by

S o u t h e r n Peninsula.

ice

final

159
F a r r a n d ’s b r y o p h y t e
approximately

site are too y o u n g

and b e l i e v e s
Creeks

13,000

of 12,500

Fu l l e r t o n

14,000 yrs.

yrs.

B.P.

B.P.,

from the C h e b o y g a n

to be e a s i l y accomodated.
reevaluated

the d e p o s i t
forest

a v e r a g i n g about

of the An tr i m C o u n t y site.

and

- 13,000

(1980)

bur ie d

is lo c a t e d

and O u t e r Port H u r o n C o m p l e x e s must

form ed b e t w e e n

estimates

(now covered)

75 km n o r t h e a s t

B e c a u s e the Inner
ha v e

bed

F a r r a n d ’s i n t e r p r e t a t i o n

m a y c o r r e l a t e wi t h the Two

in W i s c o n s i n

11,850 yrs.

B.P.;

(numerous

d at es

B l a c k and Rubin,

1967-

1968):
In view of (1) the u n c e r t a i n r e l i a b i l i t y of
c o r r e l a t i o n by means of p o l l e n spectra, (2) the 3,700ye a r range of m e a s u r e d ag e s of the C h e b o y g a n bed, (3)
the age d i s c r e p e n c i e s in d a t i n g the C a s t a l i a
bry op hytes, and (4) the p o s s i b i l i t y of isoto pe
f r a c t i o n a t i o n in some s p e c i e s of bryophytes, the age
and c o r r e l a t i o n of the C h e b o y g a n bed are c o n s i d e r e d
unproved.
R e s o l u t i o n of the age of the bed is
e x t r e m e l y i m p o r t a n t b e c a u s e the d e g l a c i a t i o n hi s t o r y ^
in the Lake M i c h i g a n and La ke H u r o n basi ns is
de p e n d e n t u p o n a s s i g n m e n t of a co rre ct age to the
b r y o p h y t e b e d ...(F u l l e r t o n , 1980, p. 20).
-r-

XXI

^

llg U L

U1

r»

UilCiDC

‘

^

4

,

L i 1 tlL > ldiU O )

J

«

m a x i m u m age of the Port H u r o n a d v a n c e
on the basis of F a r r a n d ’s b r y o p h y t e

v , _

J

M

4

u cb ciiu x ax iip ,

l

L. .

unw

in C h e b o y g a n Co un t y

site

is question abl e,

e s p e c i a l l y g iv en the ov e r l a p b e t w e e n the A n t r i m C o u n t y
and C h e b o y g a n age d et er m i n a t i o n s .
C o u n t y e st im at e
H u r o n Complex,
correct)

may

(Fullerton,
ic e- f r e e

B e ca us e the A n t r i m

record s d e g l a c i a t i o n of the
F a r r a n d ’s b r y o p h y t e da te s

in st ea d
1980),

interval.

reco rd the

In ner Port

(if t h e y are

be g i n n i n g of a Two Cre ek s

r a t h e r t h a n a Ca r y - P o r t Huron,
If so,

the till

o v e rl yi ng

the

160
bed

is G r e a t l a k e a n / V a l d e r a n

continuous

deposit

spanning

Greatlakean/Valderan
ag r e e m e n t

time.

in age

b o t h Port H u r o n and
Indeed,

among A n t r i m C o u n t y

( Gravenor and St upavsky,
a l . 1957)

morphologic

plus

the

1) st ro n g

(this study),

1976),

r a d i o c a r b o n dates

and Lake W hi tt le sey ,

ra t h e r than a

and Ohio

On ta r i o

(B ar en ds en et

for the Port H u r o n M o r a i n e

2)

the o v er al l

a c c u r a c y of

c o r r e l a t i o n b e t w e e n the A n t r i m C o u n t y site

and the type Port H u r o n ar e a

(Blewett,

1989),

in dicates

that the A n t r i m C o u n t y age e s t i m a t e may be a mo r e
re li a b l e b as is

for d e t e r m i n i n g

northern Michigan

than

provides,

first time,

for the

the Port H u r o n a d v a n c e

Conclusions

—

Prior

Port H u r o n c h r o n o l o g i e s

the b r y o p h y t e

site.

a m i n i m u m age

in

It also
estimate

for

in this pa r t of the state.

to this

study,

c o r r e l a t i o n of the

Inner and O u t e r Port H u r o n C o m p l e x e s wit h the type Port
Huron Moraine

in s o u t h e a s t e r n M i c h i g a n was b a s e d

pi-imai ily on m o r p h o l o g y .
was c o r r e l a t e d w i t h
Ontario,

Si m ii ar il y,

the la tt e r

the W y o m i n g M o r a i n e

featur e

in s o u t h w e s t e r n

and b o t h w e r e d e e m e d coev al wi th Lake W h i t t l e s e y

l a n df or m s

and

sediments throughout

Be ca u s e age d e t e r m i n a t i o n s w e r e

the Erie basin.

not a v a i l a b l e

for the

Port H u r o n C o m p l e x w i t h i n M i c h i g a n b e f o r e the r e p o r t by
F a r r a n d et a l . (1969),
O n t a r i o an d O h i o w e r e

r a d i o c a r b o n age e s t i m a t e s

a s s i g n e d to the Port H u r o n type

a r e a ba sed on these m o r p h o l o g i c
same time,

from

co rr ela ti on s,

and,

at the

a p p l i e d to the Po r t H u r o n C o m p l e x t h r o u g h o u t

161
Michigan.

Thus,

following

Port Hu ro n Co m p l e x
not verified)
This
12,960

study p r e s e n t s
B.P.

13,000

estimates,

a mi ni mu m age

for the

Inner Port H u r o n Co mp le x
given the

the C h e b o y g a n br yo ph yt e

a rel ia bl e

basis

14

C da te s

age

for e s t a b l i s h i n g

for the Port H u r o n C o m p l e x

part of the S o u th er n Pe ninsula.
1) agrees wit h

(but

a m i n i m u m r a d i o c a r b o n age of

s u r r o u n di n g
pr o v i d e s

the

r a d i o c a r b o n years old.

in no rt hw es te rn s o u t h e r n M i c h i g a n and,
co nt r o v e r s y

route,

in n o r t h e r n M i c h i g a n was a s s u m e d

to be about

+ 350 yrs.

a rat he r c i r c u i t ou s

in the nor th er n

This age d e t e r m i n a t i o n
•

fro m the W y om i n g M o r a i n e

•

in

Ontari o and with d ate s a s s o c i a t e d wi th Lake W h i t t l e s e y
Ohio,

2) helps v e r i f y L e v e r e t t

of the Port H ur on C o m p l e x
and 3)

for the first

time,

in

and T a y l o r ’s c o r r e l a t i o n

acr os s the So ut h e r n Peninsula,
establishes

the Port H u r o n C o m p l e x w i t h i n Michigan.

a m i n i m u m age

for

Chapter 5
C O N C L U S I O N S AND

I M PL IC AT IO NS

This c h a p t e r s u m m a r i z e s the sedime nto log ic,
morphologic,
they relate

and c h r o n o l o g i c
to the

fi ndings of this

Inner and O u t e r Port H u r o n complexes

in n o r t h w e s t e r n

s o u t h e r n Michigan.

discussed based

on their ve rt ica l

Landf or ms

are p r e s e n t e d

C o m pl ex es

se d i m e n ts

and

and h o ri z o n t a l

of the

Inner and O u t e r

is almost w h o l l y r e s t r i c t e d to the

contact

size.

Port Huron

1) g l a c i o f l u v i a l

2) g l a c i o l a c u s t r i n e

Post Inner Port H u r o n zone.

aspects.

findings

are a l m o s t e x c l u s i v e l y

and gravel,

S e d im en ts are

in order of d e c r e a s i n g

Sedimentologic
S u r fi ci al

st udy as

sand

silt and clay.
fluted u p l a n d s

C r es ta l

Till
and the

areas e x h i b i t

ice-

s t r a t i f i e d drift and sur fi ci al b o u l d e r s

a s s o c i a t e d w i t h d e p o s i t i o n along m a r g i n a l l y st ag n a n t
This evidence,
topography,

al on g with

indi ca te s

deposition began

the presen ce of h u m m o c k y

that

in ma n y areas o u t w a s h

in the st ag na nt zone up -i c e

marg in and e x t e n d e d

ice.

s o u t h e a s t w a r d beyo nd the

fr o m the
ice

terminus.
Me l t w a t e r d e p o s i t i o n and e r o s i o n were the do mi na nt
g e om or ph ic p r o c e s s e s o p e r a t i n g
deglaciation.

in the study a r e a during

V a r i a b l e a s pe ct s of g l a c i o f l u v i a l

de p o s i t i o n are c l e a r l y

re ve a l e d at nine grav el pits

located on the E l m i r a Plain.
162

C o m p a r i s o n s of

se diment

163
te x t u r e

and d i a g n o s t i c

transition

bedform lithofacies

fro m coarse,

poorly

d o m i n a t e d by l o n g i t u d i n a l
well-sorted braided
bedforms.
st re am s

bars,

in di ca to rs

90 d e g r e e s

parallel

axis.

to the s a n d u r

7

are

ot h e r s a n d u r
On all
the

4 1 5- 91 5

show that me l t w a t e r

to the right

interpreted

t e x t u r e d g la ci al

especially

ice

to flow

Conservative paleodischarge

mf

m sec,

these bases,

1982),

sandy

comparable

to those

from

studies.

s t r a t i f i e d drift.

Bell,

fine textured,

displaying

p r o x im al

su rf ici al

Inner and O u t e r Po r t H u r o n C o m p l e x e s

a r e a are

de po si ts

flowed p e r p e n d i c u l a r l y away from the

m a r g i n and t h e n t u r n e d

estimates

proximal

to dist al

stream deposits

Paleocurrent

first

sorted,

show a

to be p r o g l a c i a l

These
till"

but,

se di me nt s

as m a p p e d

in the

and

of

study

ic e- c o n t a c t

are not

by oth er s

in s t e a d are p r o x i m a l

im po rt a nt

se d i m e n t s

"coarse(F arrand and

facies of

he ad s of o u t w a s h g r a d e d to the

E l m i r a and O u t e r P o r t H u r o n o u t w a s h plains.
Data
that the

from w a t e r

and p e t r o l e u m well

Inn er and O u t e r Port H u r o n

an u p p e r m o s t w e d g e

of

likely

for me d by i n f i l l i n g

in ot h e r s
margin.

relief

The u p p e r m o s t

marginally stagnant

fe at u r e s

in di ca te
each contain

sand and gra ve l up to 80 m thick,

d e p o s i t e d on a m o d e r a t e
the n or th we st .

logs

till

s u rfa ce

i n c l i n e d to

sand and grav el un it s were

along

a qu as i- st ab le ,

glacial position

in some areas,

and

by d e p o s i t i o n a lo ng a s t e a d i l y r e t r e a t i n g

ice

164
Morphologic
Overall,

the t e r r a i n of b o t h the

Huron Complexes

a re as

Inner and O u t e r Port

d i s p l a y a d i s t i n c t p a t t e r n of sa li ent s

a n d reentrants.
salients

fin din gs

Th e

is c l o s e l y

l o c a t i o n a n d size of the v a r i o u s
r e lat ed to

the m a g n i t u d e

of lower

on the d e e p l y b u r i e d b e d r o c k surface.

like t he ir a s s o c i a t e d
larger

southward,

A l b a fea tur es

outside

b e g i n n i n g w i t h the

in the north,

K a l k a s k a sa lie nt
culminating

b e dr oc k lowlands,

small E l m i r a and

Grand Traverse

150 k m - w i d e

of the s t u d y area)

are p r o g r e s s i v e l y

f o l l o w e d by the l a rg er

paralleling

in a b r o a d

Salients,

s a lie nt

paralleling

Gr an d T r a v e r s e C o u n t y s o u t h w e s t w a r d

Bay,

and

(l oc a t ed

Lake M i c h i g a n from

to Wh ite hal l.

N o r t h e r n and s o u t h e r n s e c t i o n s of the st udy are a show
st r o n g c o n t r a s t i n g
d ri ft
the

thickness,

relationships

a n d the m o d e r n

topography appears

su rf ac e

landscape.

form,

In the north,

i n f l u e n c e d by hi g h b e d r o c k

rel ie f c o m b i n e d wi t h r e l a t i v e l y th i n drift.

Southward,
lower,

to be

among b e d r o c k

where drift

this

is t h i c k e r and b e d r o c k re l ie f

relationship

is absent.

In te res ti ng ly ,

the

lat te r a r e a c o i n c i d e s w i t h the b r o a d K a l k a s k a sa l i e n t and
its a s s o c i a t e d e x t e n s i v e b e d r o c k low.
that gl aci al
fl ow in g

dynamics

This

r e lat ed to thicker,

from the G r a n d T r a v e r s e

suggests

faster

ice

Ba y l o wl an d m a y help

e x p l a i n the r e l a t i o n s h i p s observed.
Twenty-six

separate

s u r f a c e s are

the M a n c e l o n a P l a i n and Post
can be gr ou pe d

into

r e c o g n i z e d wi th i n

Inner Port H u r o n

four categori es:

zone;

these

165

1. E x t e n s i v e s u r f a c e s r e p r e s e n t i n g thi ck o u t w a s h
de p o s i t s that f o r m e d along q u a s i - s t a b l e ice ma rg i n al
p o s i t i o n s of r e l a t i v e l y long d u r a t i o n (surfaces A, 1,
and 2, pl us the C r o f t o n terrace).
2. Less e x t e n s i v e su rf ac es 3-8, r e c o r di ng a br ief
int erval of fa lli ng base le ve l s cau se d by o p e n i n g of
lower ou tl e t s and c o n c o m i t a n t drops in the w a t e r table
dur in g deg la ci at io n.
3. Su r f a c e s B-Z, m a r k i n g the P l e i s t o c e n e - H o l o c e n e
t r a n s i t i o n in the C e d a r - G r e e n and J o r d a n - W a r n e r river
systems.
4. The H o f f m a n Lake Channel, re co rd in g i n ci si on
of the E l m i r a surface, and d e g l a c i a t i o n of the
e a s t e r n side of the Inner Por t H u r o n apex.
C h a r a c t e r and d i s t r i b u t i o n of some of these
is re la te d

to the

reg ion al

sa li e n t

d i s c u s s e d earlier.

Te r r a c e s

in sa lie nt

wi t h l a r g e r

regions,

l a rg er te rra ce
r e co rd long
conditions

remnants.

i n t e rv al s
fav or in g

are

and r e e n t r a n t pa t t e r n

preferentially preserved
sa li ent s

A l to ge th er ,

of q u a s i - s t a b l e

containing

these

sur fac es

ic e - m a r g i n a l

t h i c k o u t w a s h deposition,

by brief t r a n s i t i o n a l pe r i o d s

surfaces

of ra pid

punctuated

i n ci si on as the

ice m a r g i n retreated.
In a d d i t i o n to the
numerous

sm a l l e r

proximal

tra ct s

Complex es.

l a n d f or ms
of the

Th es e

are a s s o c i a t e d w i t h hu m m o c k y

Inner and O u t e r Port H u r o n

and

and

that d e g l a c i a t i o n

se ri es of s u c c e s s i v e

of sta gn an t

sedimentologic

in the

perched

ice b l o c k dep res si on s.

for the pr e s e n c e

Morphologic

fea tur es d e s c r i b e d above,

includ e h a n g i n g valleys,

d i s i n t e g r a t i o n ridges,
are e v id en ce

larg er

fans,
All

ice.

e v id en ce

in di cat es

so ut h was c h a r a c t e r i z e d by a

ice m a r g i n a l positio ns,

y o u n g e r to

166
the northwest,
areas by 1)

f o l l o we d by re a d v a n c e and burial

flu cu at io n s of the gl aci al

Port H ur on retreat,
The

terminus dur in g

or 2) G r e a t l a k e a n / V a l d e r a n advance.

1) pre se nc e of m ul t i p l e

ice ma r g i n s

in so ut he rn

sections of the O u t e r Port H u r o n Complex,
the C ro ft o n surface

of some

rel ati ve

app ar en t g r a d a t i o n of small

2) l o c a t i o n of

to these latter
in c i s e d valle ys

features,

formed at the

Inner Port H u r o n p o s i t i o n to lower surfaces

found

pro xi ma l

and 4)

to this same m a r g i n

farth er

south,

inc ision of the H o f f m a n Lake C h an ne l

in the apex region,

wi t h an absence of simil ar d o wn c u t t i n g
southward,

all

suppor t

3)

imm ed ia te ly

the

i n t e r p r e t a t i o n that the

ter minus p iv ot ed c l o c k w i s e

to the n o r th we st during

ice

deglaciation.
A l t h o u g h d e g l a c i a t i o n was
uniform,

six lines of e v i d e n c e

c o m p l e x and far from
in dicate that p r o gr es si ve

s t a g n a t i o n formed at least

9 morphosequences

5,

su r f a c e

the Lakes of the North,

and Post

land fo rm s are all
Second,

ice-contact

evidence

because

spatial a r r a n g e m e n t

First,

the

slopes and ice-con ta ct

for the pr es e n ce of sta gnant

su rf a c e s

south ea st or southwest,

1-

Inner Port Huron,

Inner Port H u r o n po si tio ns ).

ex i s t e n c e of n u m e r o u s

ice.

1,

(Margins

c o n s i s t e n t l y slope

the mo rp ho lo gy ,

of o u t w a s h

features

orientation,

and

indicate

f o r ma ti on in a s s o c i a t i o n w i t h a st agnant glacial m a r g i n
rather than is ol a t e d bl oc k s of dead
surficial

sedi me nt s

of the

ou t w a s h sand and gravel

ice.

Third,

st ud y ar e a are p r i m a r i l y

that

ex h i b it a facies chang e

167

w h i c h fines distal

to the he ad of outwash.

p r o f i l e s c o n s t r u c t e d acro ss
characteristic

distally

the ar e a show the

imbricate-like pattern delineating

morphosequences.
transition

Fourth,

Fifth,

t o p o g r a p h i c maps

in di ca te

from more c o l l a p s e d to less co l l a p s e d

from heads of outwash.

Finally,

are c o n t r o l l e d by a sp ec if ic base level.
su rfaces of the

Outwash

Inner and O u t e r Port H ur on Co mp le xe s

(Burgis,

1977);

terraces

in the Po s t

H u r o n zone may be gr a d e d to l ow er base
the above c h a r a c t e r i s t i c s
121)

terrain

morphosequences

a p p a r e n t l y are gr a d e d to the G l e n w o o d II stage
C h ic ag o

a

are

of Lake

Inner Port

levels.

All of

li s t e d by Ko t e f f

(1974,

p.

as c r i t e r i a for i d e n t i f i c a t i o n of morphose que nce s.
The

1 ) o v e r w h el m in g

i mp or ta nc e

d e p o s i t i o n and sediments,
of till,
profiles,

and 3) p re se nc e
ic e- c on ta c t

2)

of gl a c i o f l u v i a l

l a c k of s i g n i f i c a n t

of n u m e r o u s

slopes,

all uv ia l

ind icate

and O u t e r Port H u r o n C o m p l e x e s

are not c la ss ic

moraines,

but

fan-like

h a n g i n g valleys,

fans and d i s i n t e g r a t i o n rid ge s

instea d m a r k t e r r a i n

w i t h ab un da nt m e l t w a t e r and s t a g n a n t

p e rc he d

that the

formed

amounts

Inner

end

in as s oc ia ti on

ice d u r i n g

final

de glaciation.

A r e a s m a p p e d as end m o r a i n e by others

(Martin,

F a r r a nd and Bell,

1955;

hu m m o c k y pr ox im al

1982)

are ac t u a l l y

t o p o g r a p h y a s s o c i a t e d w i t h two

e s p e c i a l l y p r o m i n e n t and

im p o r t a n t heads of o u t w a s h

gr ad e d to their re sp ec t i v e

o u t w a s h plains.

168
C hr on o l o g i c
Or ga ni c mat eri al
pr oxi mal

findings

from l a c u s t r i n e deposi ts

to the Inner Port H u r o n

slope

(Antrim Cou nt y

site)

yield a IHC age d e t e r m i n a t i o n of 12,960

B.P.,

and pr ovi de

a m i n i m u m date

Port H ur on c om ple xe s

in the

located

± 350 yrs.

for the Inner and Outer

s tu dy area.

The ne ar b y Lake

Bor d e r C om p l e x wi t h an age of a p p r o x i m a t e l y 14,000 yrs.
B.P.,

co m b i n e d w i t h the A n t r i m C o u n t y date,

that the Port Hu ro n co mp le xe s p r o b a b l y
about

13,000 and

14,000 yrs.

B.P.

formed be twe en

C o n t r o v e r s i al

a ss o c i a t e d with the C h e b o y g a n b r y o p h y t e bed
13,000 yrs.

B.P.)

are

too young

indicates

dates

(12,500 -

to mark an ice-free

interval p ri or to the Port H u r o n advance,
the be gi nn in g of the Two Cr e e k s

but m a y mark

interstade.

The Antrim

Cou nt y age d e t e r m i n a t i o n 1) agr ee s with es ti ma te s
c o r r e la ti v es of the Port H u r o n Mo rai ne
O nt ari o
1976),

(Barend sen et a l ., 1957;

for

in Ohio and

G r a v e n o r and Stupavsky,

2) helps v e r i f y c o r r e l a t i o n of the Port H u ro n

Comple x w i t h i n M i c h i g a n
Blewett,

1989),

and

(Leverett and Taylor,

3) for the

first time,

m i n i m u m age on the Port H u r o n ad va n c e
part of the So u t h e r n Peninsula.

1915;

provides a

in the no rt hw e st er n

169

Suggestions
Dur in g

the c o ur se

c le a r that

for f u r t h e r re se a r ch

of this

investigation

four to pi cs w a r r a n t

(1) T r a c i n g

the E l m i r a P l a i n

ad di ti on al

it became

considera tio n.

s o u t h w e s t w a r d to the

G l e n w o o d s h o r e l i n e m a y e s t a b l i s h preci se r e l a t i o n s h i p s
b e t w e e n the Inn er Port H u r o n C o m p l e x and Lake Chicago,
and also hel p
of glacia l

in i n t e r p r e t i n g

l a n d fo rm s

in G r a n d Traverse,

and M a n i s t e e Count ies .
ar ea

is complex,

in vestigation.
am ong

fluvial

gradients,
valuable

and

the c o m p l i c a t e d as se m b l a g e

(2)

Drainage

poorly understood,

terraces,

Holocene

stream patterns

remain

s tu dy

im p o r ta nt

two

feature s exist)

to a ny such study.

and

and

(4)

C o m p l e x bo th to the east

d e p o s i t i o n along

the

there

sou the rn

is a full and

sur fa ce s

stratigraphic
research.

3,

s o ut h will

4, and

ma y

re l a t i o n s h i p s

Distinguishing

In ne r Port H u ro n C o m p l e x e s

to the

is p o o r l y u nd er st ood ;

development.

fr om a m i n o r re advance,

in this

b e t w e e n the M a n i s t e e

mi gh t pr ovi de

in n o r t h w e s t e r n

in the a r e a wh ere

key m o r p h o l o g i c

w h i c h are

and pi ra c i es

river

of G r e a t l a k e a n / V a l d e r a n events.

5 are bur ie d by d e p o s i t s
rev ea l

lake levels,

i n c o m p l e t e u nt il

accurate understanding
field

in the

and w a r r a n t s

into Q u a t e r n a r y land sc ap e

(3) The d e g l a c i a t i o n c h r o n o l o g y

Detailed

evolution

Benzie,

A d e t a i l e d a n a l y s i s of re la ti o n s h i p s

in si gh ts

M i c h i g a n will

Wexford,

(if

l i k e l y be central

The c h a r a c t e r of the Po rt Hu ro n
and

so u t h we st

investigating
fe at ur e

mig ht

of the

st udy area

the c h a n g i n g modes of
provid e

a better

170
understanding

of gl a c i a l

landforras

in this par t

of

Michigan.
Finally,
Rieck

(1976),

demonstrate

published

and o t h e r

Burg is

recent

(1977),

the u s e f u l n e s s

geomorphology
landscape.

this

studies

an d B l e w e t t and R i e c k

of r e s e a r c h on reg io na l

since L e v e r e t t

very

few reports

of glaci al

g ive n rece nt

have been

and T a y l o r ’s 1915 m o n o g r a p h and

lit tl e d e t a i l e d m a p p i n g has b e e n done.

imp or tan t

sediments

concerns

An a c c u r a t e

is e s p e c i a l l y

regarding

groundwater

c o n t a m i n a t i o n and h a z a r d o u s w a s t e disposal.
far behi nd a d j o i n i n g
and

i n t e r p r e t in g

states

and O n t a r i o

addressing

these

S u r v e y D i v i s i o n or the

S u r v e y w o u l d be a m a j o r
.inadequacies.

is

and landforms.

f u n d e d b y the D e p a r t m e n t

Na t u r a l R e s o u r c e s ’ G e o l o g i c a l
Geological

Michigan

in d o c u m e n t i n g

its Q u a t e r n a r y se di me nt s

A reg ional m a p p i n g program,

U.S.

(1987)

in u n d e r s t a n d i n g M i c h i g a n ’s g l a c i a l

U nf or t u n a t e l y ,

understanding

incl ud in g

first

step in

of

APPENDICES

APPENDIX A

F IEL D AND L A B O R A T O R Y T EC HN IQ UE S

F IE LD TE CH NI Q U E S
G R A V E L PITS AND O T H E R EXPO SU RE S
Nine gravel pits c o n t a i n i n g
least

3 m high and 3 m wide were

te ch ni qu es

fresh ve rt ic al
sampled using

faces at
the

d e s c r i b e d below:

Sand and gravel
1. Four l o c at io n s w i t h i n each pit were ch o s e n at
rand om u sin g a b o a r d game spinner.
2. An e x c a v a t i o n a p p r o x i m a t e l y one m e t e r long by
two me t e rs h i g h was made 1.5 m below the top of the
face at each of the four sites.
A b se nc e or
pre se nc e of be ddi ng was recorded, as were details
of sediment type and s t ra ti gr ap hi c association.
3. A two m e t e r v e r t i c a l sample (Krumbein and
Pettijohn, 1938) was t a k e n and dumped at a
p r e d e t e r m i n e d c o l l e c t i n g area.
4. S ubs am ple s from all four areas we r e m i x e d
t oget her at the c o l l e c t i o n site and to gether
formed the m a i n sam pl e for that site.
5. Fine t e x t u r e d s e d i m e n t s ( < 8 mm) were c o l l e c t e d
by ten ra nd om hand grabs and label ed for later
sieving in the laboratory.
6. S e v e n t y - f i v e c o a r s e ( > 8 mm) fragments were
sampled u sin g a w i r e grid p l a c e d atop the
c oll e c ti ng pile.
7. Princ ipa l axis lengt hs (in cm) were m e a s u r e d and
recorded for lat er te xt ur e ana lys is and sp he ri ci ty
study.
R o u n d n e s s was d e t e r m i n e d v i s u a l l y usi ng a
s tan da rd set of g r a i n images (Leeder, 1982).
8. Clasts we r e th e n c l a s s i f i e d based on lithology.
Those rocks of u n k n o w n o r i g i n were c o l l e c t e d for
lab or a to ry study.
172

173

In addition,
measured

o r i e n t a t i o n of

im bri cat ed

stones was

in order to d e t e r m i n e p a l e o c u r r e n t s .

These

m e a s u r e m e n t s were t ak en w h e r e o r i e n t a t i o n was best
d e v e l o p e d or w he re the
accessible.

face of the exp osu re was most

O r i e n t a t i o n and dip of 50 e l o n g a t e d clasts

(3:1 a-b ratio,

m i n i m u m a-axis

l e n g t h 1 cm)

were

recorded.

Till -least

I de nt if i a bl e

tills were

s a mpl ed

from at

three pla ces w i t h i n the till mass and m i x e d

to g e t h e r to form a sample.

Two

such samples were

co l l e c t e d and tag ge d for later a n a l y s i s

in the

laboratory.

S U R F I C I A L S E D I M E N T STUDY
S ur fic ia l

se diment

s tu dy c o n s i s t e d of 1) bo ul de r

mapping,

and 2)

B o ul d e rs

-- Ba sed on road r e con na iss an ce,

three

sa mpl in g

or more bo u l d e r s

100-150 met ers

Ornamental

o ri g i n we r e not
Field

the

shape

recorded,

(angular,

ex is t wit hi n
as were

su b- angular,

bo ul d e r s or t h o s e of q u e s t i o n a b l e

included.

stone pi les

determined

p l a c e s where

>50 cm in b - d i a m e t e r

of one an ot he r we r e

l i t h o l o g y and o v er all
round).

of field stone piles.

-- All

r e c o g n i z a b l e stone p i l e s

from road r e c o n n a i s s a n c e )

following met hodolo gy:

(as

were s a m p l e d using

174

1. Two se parate poi nt s w i t h i n a stone pile were
cho sen at ra nd o m using a spinner.
2. A rec ta ng ul ar grid was c e n t e r e d ov e r each point
and 25 stones collected,
3. Stones from the two sites were then m ix ed
to get he r to form a samp le of 50 stones.
4. Princ ipa l axes, roundness, and l i t h o l o g y of
individual stones we r e d e t e r m i n e d in the field.
Stones of un k n o w n l i t h o l o g y were br ou gh t to the lab
for further analysis.

L AB OR A T O R Y TE CH NI Q U E S
SAND AND G R A V E L
Fine

tex tur ed mat er ia l

(<8 mm)

-- Sieving

follows the

sta nda rd m e t h o d o l o g y d e s c r i b e d by K r u m b e i n and Pett ij oh n
(1938)

and by Folk

fragm ent s

( >8

mm)

(1974)

but d i f f e r s

were m e a s u r e d

in the

the m e t h o d o l o g y a l re ad y di scussed.
the large

sample

sizes o t h e r wi se

in that coarse st
field based on

This m e th od avoids

r e qu ir ed due to the

c oa rs en es s of the material.
Fine tex tu re d
two subsaraples,

samples

( <8

mm)

were d i vi d e d

one serving as backup.

into

70 grams of the

m a i n sample were w e i g h e d and s e p a r a t e d using nes te d
sieves

fol low ing

st and ar d p r oc ed ure s.

then w e i g h e d and a re lative p e r c e n t a g e

Each separat e was
for each category

calculated.
Sp h e r i c i t y -- S p h e r i c it y me a s u r e s

re lative c o mp a c t n e s s of

a rock and

of me ch a n i c a l

is an indirect m e a s u r e

a rock fragment.
uses

This

study fo ll ow s Ch ur c h

fo llowing measure:
I_____
S =.bc/a1 ( K r u m b e i n ’s in t e r c e p t

wear upon

(1972)

the

sphericity)

and

175

whe re

a,

Valu es

b,

an d c are p r i n c i p a l

axes and S = sphericity.

from ea c h l o c a t i o n we re m a p p e d to d e t e r m i n e

spatia l v a r i a b i l i t y a c ro ss

the

sandur.

TILL
Texture

-- Till wa s

fr a ct io ns

us ing

separated

a 2 m m sieve.

into coar se and
Fine

tex tu re d ma t e r i a l was

then a n a l y z e d by h y d r o m e t e r b a s e d on the
(Indorante,

et a l .,

fine

following method

1990):

1. A 50 g r a m s a m p l e was p l a c e d in a fleaker,
dried, d e s s i c a t e d , c o o l e d and reweighed.

oven

2. Te n ml of 5% s o d i u m h e x a m e t a p h o s p h a t e was added
to the fleaker.
The f l e a k e r was then fi l le d to 1/3
to 1/2 full.
3.
12

The f l e a k e r was c a p p e d and put
h ou rs at low to m e d i u m speed.

in a shaker for

4. The s o i l / l i q u i d m i x t u r e in the fleake r was
w a s h e d into a n d t h r o u g h a 53 u m sieve into a 1000
ml s e t t l i n g cy linder.
5. Sand in the 53 u m sieve was wa s h e d into a
b e a k e r and o v e n dried.
Th i s sample wa s cooled,
de ss icated, a n d weighed.
6. The s e t t l i n g c y l i n d e r was filled w i t h d i s t i l l e d
w a t e r to the 1000 ml m a r k and pl a c e d in a
t e m p e r a t u r e c o n t r o l l e d r o o m overnight.
7. The m i x t u r e in the c y l i n d e r was then a g i t a t e d
for 30 seconds.
8. The m a t e r i a l in s u s p e n s i o n was then m e a s u r e d
us in g a h y d r o m e t e r .
T i m e s for h y d r o m e t e r re adings
we r e d e t e r m i n e d b as ed on temperature.
Rea di ng s
we r e t a k e n for ea c h sample as well as for a blank.
9. P e r c e n t a g e s of sand, silt and clay w e r e
d e t e r m i n e d for e a c h sample.

Col or

-- C o l o r of m o i s t

each sample u s i n g

and d r y sampl es were

Munsell

c o l o r charts.

then

recorded

for

APPENDIX B

CLAY MINEROLOGY

M i n e r o l o g y of t il ls was e x a m i n e d using X - r a y
d i f f r a c t i o n of o r i e n t e d cl a y
(no date).
milliamps

Samples were
between

fo l l o wi ng Glass

30 KV and

15

2 t he ta at a sc a n rate of

Peak and b a c k g r o u n d c o u n t s

c a l c u l a t e d by computer.
in triplicate.

50),

s c a n n e d at

5-14 d e g r e e s

1 de gr e e per minute.

run

(Fig.

E a c h of the

11 rill

Preparation procedures

were

sa mpl es were

are d e s c r i b e d

below:
1. T w e n t y - f i v e grams of sa m pl e were a d d e d to a 300
ml fleake r and top pe d out w i t h a p p r o x i m a t e l y 150 ml
of d i s t i l l e d water.
2. The f l e a k e r (with cap on)
by hand for 1 minute.

was sha ke n v i g o r o u s l y

3. In one q u i c k m o t i o n a p p r o x i m a t e l y 100 ml of the
mi x t u r e was p o u r e d into a 100 ml b e a k e r and the
r e m a i n d e r of the s o i l / w a t e r s u s p e n s i o n was
discarded.
,4. The b ea k e r was c o v e r e d and allow ed
•overnight to a l l o w floccu la ti on .

to

sit

5. If the c l e a r s u p e r n a t a n t w as d i s t i n g u i s h a b l e the
next day, it w a s s i p h o n e d off and the b e a k e r was
r e f i l l ed w i t h d i s t i l l e d water, v i g o r o u s l y stirre d
for one m i n u t e w i t h a c l e a n glass rod, a nd al lo we d
to sit o v e r n i g h t again.
This was r e p e a t e d until
the s u p e r n a t a n t r e m a i n e d so me w h a t c l o u d y a f t e r 24
hours.
One t hi rd of the so l u t i o n was t h e n si ph on ed
off and the b e a k e r t o p p e d off wi t h d i s t i l l e d water.
6. Two dr ops
the beaker.

of a 10% C a l g o n

176

s o lu ti on w e r e

added to

177
7. The s o l u t i o n was hand m i xe d for 1 m i n u t e w i t h a
s t i r r i n g rod and then a l l o w e d to stand for 15
minutes.
8. An e y e - d r o p p e r full of s o l u t i o n was d r a w n off
(as m u c h as p o s s i b l e in one motion) from the top of
the s o l u t i o n and a p p l i e d to glass p e t r o g r a p h i c
slides.
The w h o l e slide was c o v e r e d by s p r e ad in g
out the liquid with the top of the d r o p p e r and the
slide was kept level t h r o u g h o u t the process.
9. The slide was a l l o w e d
for one day.

177

to d r y at r o o m t e m p e r a t u r e

6.0

8.0 ‘

10.0

12.0

d e g re e s 2 theta

Figure 50. X-ray diffractograms.

1.4.0

vo.®
8.®

degi®oS

oia
it'd-V

Figure50- ^con

180
SAM PLE #

i

6.0

i

i

1

8.0

i

10.0

dogroes 2 Uioia

Figure 50. (cont'd.).

12.0

14.0

LIST OF R E FE RE NC ES

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ICE-CONTACT AND PROGLACIAL STRATIFIED DRIFT ASSOCIATED
WITH ICE-MARGINAL POSITIONS AND PROXIMAL AREAS OF
OUTWASH PLAINS. USUALLY CONTAIN DEFORMED
GLACIOFLUVIAL SAND AND GRAVEL, GLACIOLACUSTRINE SILT AND CLAY, LIMITED AMOUNTS
O F FLOW TILL, AND BOULDERS NEAR ICE
MARGINAL POSITIONS. ELSEWHERE,
EXHIBIT COARSE, GRAVEL-DOMINATED
BEDFORMS OF PROXIMAL MELTWATER
STREAMS PLUS SILT AND CLAY DRAPES.

R8W

TRANSITIONAL, MEDIAL AND DISTAL
PROGLACIAL SAND AND GRAVEL
BEDFORMS ASSOCIATED WITH
OUTWASH PLAINS. ALSO
CONTAIN SCATTERED ICECONTACT SEDIMENTS
RELATED TO ICE BLOCK
DEPRESSIONS, AND
EOLIAN DEPOSITS
ASSOCIATED WITH
DUNES.

RUGG POND -»■

GLACIOLACUSTRINE
SAND, SILT,
AND CLAY.

R 7 W

Qt

TILL, UNDIFFEREN­
TIATED
KALKASKA

R 6 W

T 2S'i

T 26 N

Figure 15.
Map of the surficial sedim ents of
the Inner and Outer Port Huron Complexes, northwestern southern Michigan.
-------------------------- 7—

Qpg

RUGG POND
SITE

ANT
RO/
GR/

Q ic

Qpg'

N

Q ic

^----------------------------------- <r~

Q ic

Qpg

Q t Ql

Q pg

MANCELONA

Qpg

Q ic

Qpg

Q ic

KALKASKA

Qpg

Q ic

Qpg

.X

T 27 N

T 28 N

BOULDER
C O N C E N T R A T IO N S

PRINCIPA L
GRAVEL, SAND,
OR CLAY PIT

PR IN C IP A L
IC E -M A R G IN A L
P O S IT IO N S

CITY O R
VILLAGE

1 COUNTY
COMMISSION
L PIT

Q ic
Q ic

QP9

Q ic

ELMIRA

XX

Q ic

Q ic

Qpg

Q ic

Qpg

SCALE
R.F. = 1 :1 5 6 ,2 5 0

T 30 N

T 31 N

Elk L a k e

FIGUR E 3 2 . L A N D F O R M S O F T H E INN ER
AND OUTER PO RT H U R O N C O M PLEXES

■

Lake
Skegemog

ICE-MARGINAL POSITIONS
FLUTED UPLANDS, SHOWING
INFERRED DIRECTION OF
ICE MOVEMENT
DIRECTION OF
MELTWATER
DRAINAGE

R.F.=1:156,250

uncontrolled disintegration

(S u rfa c e s 1 a n d 2 com bined)

R 7 W

KALKASKA

disintegration
ridges

CROFTON
SU R FA C E

R 6 W

OUTER

T 26 U

p

Torch Lake
L a ke B e lla ire

Up
Os
Lake o l
th e W o o d s

t a k e o l th e
W o o d s P lain

s X-Y-2
disintegration
rid g e s

s m a ll in c is e d
v alley s

^

—
SU RFA CE A

MANCELONA
S a tte rly L a k e

ALBA
M ancelona R eentrant

<ASKA

ALBA SURFf''G'£> /^ ^
Alba
South
Apron
Alba Salient

I—
ORT

”

**-T-

HURON

T 27 N

LAKES O F THE

C O M P L E*

T 28 N

T 29 N

noh^

T H R O U G H

A N D

V A L L E Y S

disintegration
ridges
S U R FA C E A
A

J o rd a n

A*

/

)b.

Deadman's
Hill

ELMIRA

Hoffman Lake
Channel

kettle
chains

8

A PV>

CAMP

!A S U R F A * ^

A bandoned

Farm

Hummocks

Elmira
South
Apron

ten

S U R F ^ ' ^ l / ^ ' ^ D isin teg ratio n R i d g e s \

W^ourep

Alba Salient

Lake 27
Disintegration R idges

:S O F TH E N O R ^ ^

OUT
X
T 30 N

T 31 N